Geological Survey of Denmark and Greenland Bulletin 19 ... - Geus

GEOLOGICAL SURVEY OF DENMARK AND GREENLAND BULLETIN 19 2009
Lithostratigraphy of the
Cretaceous–Paleocene Nuussuaq Group,
Nuussuaq Basin, West Greenland
Gregers Dam, Gunver Krarup Pedersen, Martin Sønderholm,
Helle H. Midtgaard, Lotte Melchior Larsen, Henrik Nøhr-Hansen
and Asger Ken Pedersen
GEOLOGICAL SURVEY OF DENMARK AND GREENLAND
MINISTRY OF CLIMATE AND ENERGY

Geological Survey of Denmark and Greenland Bulletin 19
Keywords
Lithostratigraphy, Nuussuaq Group, Cretaceous, Paleocene, West Greenland, Nuussuaq Basin.
Cover illustration
Sedimentary succession of the Nuussuaq Group at Paatuut on the south coast of Nuussuaq, one of the classical localities for sedimentological
and palaeontological studies. The photograph shows deep incision of the Paleocene Quikavsak Formation into the Upper
Cretaceous Atane Formation. The conspicuous red coloration is due to self-combustion of carbonaceous sediments. The upper part
of the succession comprises volcanic rocks of the West Greenland Basalt Group. The height of the mountains is c. 2000 m. Photo:
Martin Sønderholm.
Frontispiece: facing page
View down into the narrow Paatuutkløften gorge on the southern coast of Nuussuaq, where coarse-grained, pale sandstones of the
Paleocene Quikavsak Formation fill a major incised valley cut into interbedded mudstones and sandstones of the Cretaceous Atane
Formation. Sea-fog often invades the coastal valleys but typically dissipates during the day. Photo: Finn Dalhoff.
Chief editor of this series: Adam A. Garde
Editorial board of this series: John A. Korstgård, Geological Institute, University of Aarhus; Minik Rosing, Geological Museum, University
of Copenhagen; Finn Surlyk, Department of Geography and Geology, University of Copenhagen
Scientific editor of this volume: Jon R. Ineson
Editorial secretaries: Jane Holst and Esben W. Glendal
Referees: J. Christopher Harrison (Canada), Robert Knox (UK) and T. Christopher R. Pulvertaft (Denmark)
Illustrations: Jette Halskov
Digital photographic work: Benny M. Schark
Layout and graphic production: Annabeth Andersen
Printers: Rosendahls . Schultz Grafisk a/s, Albertslund, Denmark
Manuscript submitted: 22 April 2008
Final version approved: 1 September 2009
Printed: 28 December 2009
ISSN 1604-8156
ISBN 978-87-7871-260-8
Citation of the name of this series
It is recommended that the name of this series is cited in full, viz. Geological Survey of Denmark and Greenland Bulletin.
If abbreviation of this volume is necessary, the following form is suggested: Geol. Surv. Den. Green. Bull. 19, 171 pp.
Available from
Geological Survey of Denmark and Greenland (GEUS)
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Contents
Abstract . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Preface . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Introduction. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Previous work. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
The period before 1938 – the pioneers on the fossil floras . . . . . . . . . . . . . . . . . . . . .
The Nûgssuaq Expeditions 1938–1968 . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
The early hydrocarbon and coal-related studies 1968–1982 . . . . . . . . . . . . . . . . . . . .
Recent investigations . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Geological setting . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Nuussuaq Group. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Kome Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Slibestensfjeldet Formation. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Upernivik Næs Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Atane Formation. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Skansen Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Ravn Kløft Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Kingittoq Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Qilakitsoq Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Itivnera Bed . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Itilli Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Anariartorfik Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Umiivik Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Kussinerujuk Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Aaffarsuaq Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Kangilia Formation. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Annertuneq Conglomerate Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Oyster–Ammonite Conglomerate Bed . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Quikavsak Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Tupaasat Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Nuuk Qiterleq Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Paatuutkløften Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Agatdal Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Eqalulik Formation. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Abraham Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Atanikerluk Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Naujât Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Akunneq Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Pingu Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Umiussat Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Assoq Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Acknowledgements . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
References . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Appendix: Place names and localities . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
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4

Abstract
Dam, G., Pedersen, G.K., Sønderholm, M., Midtgaard, H.H., Larsen, L.M., Nøhr-
Hansen, H. & Pedersen, A.K. 2009: Lithostratigraphy of the Cretaceous–Paleocene
Nuussuaq Group, Nuussuaq Basin, West Greenland.
Geological Survey of Denmark and Greenland Bulletin 19, 171 pp.
The Nuussuaq Basin is the only exposed Cretaceous–Paleocene sedimentary basin in West Greenland
and is one of a complex of linked rift basins stretching from the Labrador Sea to northern Baffin
Bay. These basins developed along West Greenland as a result of the opening of the Labrador Sea
in Late Mesozoic to Early Cenozoic times. The Nuussuaq Basin is exposed in West Greenland between
69°N and 72°N on Disko, Nuussuaq, Upernivik Ø, Qeqertarsuaq, Itsaku and Svartenhuk Halvø
and has also been recorded in a number of shallow and deep wells in the region. The sediments
are assigned to the more than 6 km thick Nuussuaq Group (new) which underlies the Palaeogene
plateau basalts of the West Greenland Basalt Group. The sediment thickness is best estimated from
seismic data; in the western part of the area, seismic and magnetic data suggest that the succession
is at least 6 km and possibly as much as 10 km thick. The exposed Albian–Paleocene part of
the succession testifies to two main episodes of regional rifting and basin development: an Early
Cretaceous and a Late Cretaceous – Early Paleocene episode prior to the start of sea-floor spreading
in mid-Paleocene time. This exposed section includes fan delta, fluviodeltaic, shelfal and deep
marine deposits.
The Nuussuaq Group is divided into ten formations, most of which have previously been only
briefly described, with the exception of their macrofossil content. In ascending stratigraphic order,
the formations are: the Kome Formation, the Slibestensfjeldet Formation (new), the Upernivik
Næs Formation, the Atane Formation (including four new members – the Skansen, Ravn Kløft,
Kingittoq and Qilakitsoq Members – and one new bed, the Itivnera Bed), the Itilli Formation
(new, including four new members: the Anariartorfik, Umiivik, Kussinerujuk and Aaffarsuaq
Members), the Kangilia Formation (including the revised Annertuneq Conglomerate Member and
the new Oyster–Ammonite Conglomerate Bed), the Quikavsak Formation (new, including three
new members: the Tupaasat, Nuuk Qiterleq and Paatuutkløften Members), the Agatdal Formation,
the Eqalulik Formation (new, including the Abraham Member), and the Atanikerluk Formation
(new, including five members: the Naujât, Akunneq (new), Pingu (new), Umiussat and Assoq (new)
Members).
Authors’ addresses
G.D., DONG Energy, Agern Allé 24–26, DK-2970 Hørsholm, Denmark. E-mail: greda@dongenergy.dk
G.K.P., Department of Geography and Geology, University of Copenhagen, Øster Voldgade 10, DK-1350 Copenhagen K,
Denmark. E-mail: gunver@geol.ku.dk
M.S., Geological Survey of Denmark and Greenland. Present address: DONG Energy, Agern Allé 24–26, DK-2970 Hørsholm,
Denmark. E-mail: mason@dongenergy.dk
H.H.M., DONG Energy, Agern Allé 24–26, DK-2970 Hørsholm, Denmark. E-mail: helmi@dongenergy.dk
L.M.L., Geological Survey of Denmark and Greenland, Øster Voldgade 10, DK-1350 Copenhagen K, Denmark.
E-mail: lml@geus.dk
H.N.-H., Geological Survey of Denmark and Greenland, Øster Voldgade 10, DK-1350 Copenhagen K, Denmark.
E-mail: hnh@geus.dk
A.K.P., Natural History Museum of Denmark, University of Copenhagen, Øster Voldgade 5–7, DK-1350 Copenhagen K,
Denmark. E-mail: akp@snm.ku.dk
5

Preface
The onshore Cretaceous–Paleocene sedimentary succession
of the Nuussuaq Basin in West Greenland has been
studied since the mid-1850s, mainly because of its
extremely well-preserved macroplant and invertebrate
fossils and the presence of coal. The early work suggested
major age differences between the various lithological
units, but as knowledge increased as a result of the investigations
carried out from the late 1930s to the late 1960s,
the time gaps gradually diminished. During this period,
several more or less informal stratigraphic schemes evolved
and were even used differently by different authors, causing
confusion concerning the actual definition, the vertical
and lateral extent, and the age of the lithological units.
This confusion was not helped by the fact that spelling
conventions regarding Greenlandic place names changed
considerably over time. No formal lithostratigraphy in
the Nuussuaq Basin was defined, although Troelsen
(1956) in his overview on stratigraphic units in Greenland
treated the units he described as formal.
In the early 1990s, focus was again directed towards
the region as an analogue for the offshore basins of West
Greenland. The Danish State, and later the Greenland
Government, provided substantial funding for studies that
could counter the general assessment of the region as
being only gas-prone. Both extensive acquisition of seismic
data and substantial onshore field studies were initiated
in the Nuussuaq Basin during this period under
the auspices of the Geological Survey of Greenland (from
1995 the Geological Survey of Denmark and Greenland,
GEUS). During the following years, the Nuussuaq Basin
evolved from being an analogue for the offshore areas to
being an exploration target in itself due to the finds of
widespread oil seeps in the basin resulting in the drilling
of the first onshore exploration well in Greenland in1996.
This culminated in 2007 when petroleum exploration
offshore Disko took a major leap forward with the granting
of seven new exploration licenses. It is therefore evident
that a formal description of the thick and varied
succession onshore is strongly needed in order to create
a common reference for geoscientists working in the
region.
The authors have contributed to various extents in
the completion of the manuscript. Gregers Dam, Gunver
Krarup Pedersen and Martin Sønderholm have had dual
roles as authors and compilers. They have provided original
data on most of the formations, have written the introductory
chapters and have supplied the majority of the
figures. They have been responsible for the manuscript
in all stages and have revised the manuscript in accordance
with the comments from the referees. Helle H.
Midtgaard has provided sedimentological logs and original
observations on the Kome, Slibestensfjeldet and
Upernivik Næs Formations and on the Ravn Kløft
Member of the Atane Formation. Henrik Nøhr-Hansen
has examined numerous palynological slides and has provided
data on the ages of most of the formations. Lotte
Melchior Larsen and Asger Ken Pedersen have made it
possible to correlate the siliciclastic sediments of the
Atanikerluk Formation to the co-eval magmatic rocks,
and have documented the areal extent of sedimentary and
volcanic rocks on maps and vertical sections.
7

■
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■
■
■
■
■
■
■
■
■
■
70°W
■
■
60°W 50°W
■
■
■
■
200 km
■
■
74°N
■
■
■
Melville
Bay
■ ■
■
■
■
■
■
■ ■
■
■
■ ■ ■ ■
Greenland
Baffin
Bay
■ ■
■
■
■
■
Greenland
Possible oceanic crust or
attenuated continental crust
■
■ ■
S
■
■
Mesozoic basin
Palaeogene volcanic rocks
■
■
70°N
■
■
■
■
■
■
N
■
Shallow or exposed
continental basement
Exploration wells
■
■
■
D
■
70°N
Exploration wells 1976–1977
■ ■
■
■
■
■
■
■
■
Nuussuaq
Basin
■
Faults
C
Davis
Strait
■
■
■
■
■
■
■
■
■
66°N
■
■
■
■
■
66°N
■
■
■
■
■
Labrador
Sea
■
■
■
■
■
■
■
■
■
■
■
■
60°W 50°W
■
■
■ ■
■
■
■
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■
Fig. 1. Simplified geological map of West
Greenland (for location, see inset) showing
the Nuussuaq Basin in its regional setting,
broadly outlined by the red box. Based on
Escher & Pulvertaft (1995), Chalmers &
Pulvertaft (2001), Oakey (2005) and
Gregersen et al. (2007). C, Cape Dyer; D,
Disko; N, Nuussuaq; S, Svartenhuk Halvø.
8

Introduction
The Nuussuaq Basin belongs to a complex of basins that
were formed in the Early Cretaceous, extending from
the Labrador Sea in the south to Melville Bay in the
north (Fig. 1; Chalmers & Pulvertaft 2001). Due to local
uplift during the Neogene, it is the only one of these
basins that extends into the onshore area in West
Greenland where Upper Cretaceous – Paleocene sediments
overlain by volcanic rocks can be studied in the
Disko – Nuussuaq – Svartenhuk Halvø area. The Nuus -
suaq Basin has therefore been used for many years as an
analogue for the basins offshore southern and central
West Greenland, the primary target for petroleum exploration.
The former lithostratigraphy of the Nuussuaq Basin
was established by researchers working with the classic
flora and fauna of the Nuussuaq Basin, and definition
of lithostratigraphical units was therefore to a large extent
governed by fossil finds. This resulted in an incomplete
lithostratigraphical scheme comprising some ill-defined
units which were not true lithostratigraphic units.
During the last two decades, the sedimentology, bio -
stratigraphy, sequence stratigraphy and organic geo-
55°W
Hareøen
70°N
Maligaat
Itilli
Fig. 65
Fig. 44
Fig. 74
Ilugissoq
Alianaatsunnguaq
Fig. 82
Aaffarsuaq
Ikorfat
Fig. 113
Naassat
Nuuk Killeq
Nuuk Qiterleq
Tupaasat
Fig. 22
Paatuut
Kussinerujuk
Kuugannguaq Asuk
Qorlortorsuaq
FP93-3-1
Qullissat
Stordal
Vaigat
Qaarsut
Fig. 21
Ak
EIQ
Ataata Kuua
Saqqaqdalen
Uummannaq
Atanikerluk
Nuussuaq
Fig. 40
Saqqaq
51° W
55°W
72°N
71°N
70°N
Svartenhuk
Halvø
Ubekendt
Ejland
Qeqertarsuaq
Fig. 73
Disko
Upernivik Ø
Fig. 33
Nuussuaq
Vaigat
51°W
Inland
Ice
Disko
Sorte Hak
Pingu
69°N
Grønne Ejland
50 km
Aasiaat
West Greenland Basalt Group
Uiffaq
Skansen
Assoq
Fig. 124
25 km
Skarvefjeld
Qeqertarsuaq
Ilulissat
Disko Bugt
55°W 51°W
Precambrian basement
Nuussuaq Group
Town
Locality
Fig. 2. Map of Disko and Nuussuaq showing the main localities and place names used in this paper. Frames and figure numbers indicate coverage
of detailed maps and a seismic section. The pre-Quaternary geology is simplified from Escher (1971). The detailed maps of Upernivik
Næs (Fig. 33) and Svartenhuk Halvø – Qeqertarsuaq (Fig. 73) are located on the regional map on the right. Ak, Akuliarusinnguaq; EIQ,
Eqip Inaarsuata Qaqqaa.
9

Fig. 3. Topographical map by Rink (1857) reproduced by Nordenskiöld (1871), showing the location of Kome, Atane and other named features
given lithostratigraphic significance by Nordenskiöld.
10

chemistry of the Nuussuaq Basin have been studied in
detail by the Survey and the University of Copenhagen,
and it is now possible to establish a modern, formal,
lithostratigraphic framework for all the sedimentary units
in the Nuussuaq Basin. As now defined, the individual
Cretaceous – Early Paleocene formations are, to a large
extent, genetic units bounded by unconformities. The
new framework has been established with the least possible
alteration of the earlier defined units in order to avoid
confusion and to promote the overall understanding of
the basin. Therefore, the naming of units does not in all
cases conform to the rules set out by the North American
Commission on Stratigraphic Nomenclature (1983).
Some of the old informal units were named according
to their content of fossils or lithology; a few of these
units have been retained due to the large collections of
fossils originating from them.
The place names used herein are all in modern
Greenlandic orthography. However, previously defined
lithostratigraphic units using older spelling have not been
renamed. A complete list of place names used is given
in both new and old orthography in the Appendix; their
location is shown on Fig. 2.
Previous work
The period before 1938 – the pioneers
on the fossil floras
The Cretaceous–Paleocene sediments of West Greenland
have been known as far back as the time when the
Norsemen in Greenland visited this area and named a
headland ‘Eysunes’ from the Norse word ‘eisa’ (meaning
glowing embers); this refers to the spontaneous combustion
of organic-rich mudstones and coal that has
taken place after landslides at several localities along
Vaigat, the strait between Disko and Nuussuaq (Fig. 2;
Rosenkrantz 1967; Henderson 1969).
Following re-colonisation in 1721, the coal seams
along Vaigat again attracted much attention, and by the
time the region had its first inspector in 1782 the Disko
Bugt colonies had become self-sufficient in coal, as mentioned
in Paul Egede’s ‘Efterretninger om Grönland’
(Steenstrup 1874). The early geological and geographical
investigations of this region were reported by Giesecke
(1806–13, in: Steenstrup 1910), Rink (1853, 1857; Fig.
3), Nordenskiöld (1871, 1872) and Brown (1875). An
account of the later investigations up to 1968 can be
found in Rosenkrantz (1970).
For many years it was plant fossils found in the limnic
part of the succession that attracted the attention of geologists
from all over the world. Brongniart (1831 p. 351)
described the first species from Kome on northern
Nuussuaq. In the following years, collections of plant
fossils were made at several localities in the region, mainly
from eastern Disko and Atanikerluk, which were described
by Heer (1868). These descriptions aroused so much
interest that a British expedition led by E. Whymper
and R. Brown was sent out to collect new material in 1867
(Heer 1870). The expedition of A.E. Nordenskiöld in
1870 provided a much larger collection, and for the first
time Upper Cretaceous strata were recognised (Heer
1874a, b). Collections from an expedition in 1871 led
by E.G.R. Nauckhoff were described by Heer (1880).
Important new collections were made by K.J.V. Steenstrup
during his expeditions in 1871–72 and 1878–80, and
members of Steenstrup’s expeditions discovered a number
of new plant fossil localities on Disko, Nuussuaq,
Upernivik Ø and Svartenhuk Halvø (Fig. 4). Steenstrup
brought his collection back to Copenhagen in 1880 and
it was described by Heer (1882, 1883a, b). Heer (1883b)
concluded from his studies, which now included more
than 600 species (e.g. Fig. 5), that the plant fossils could
be divided into three Cretaceous floras (the Kome, Atane
and Patoot floras) and one flora of Tertiary age (the Upper
Atanikerdluk flora).
Later work on plant fossils from this area includes
that of Seward (1924, 1926), Miner (1932a, b; 1935),
Seward & Conway (1935, 1939), Koch (1963, 1964,
1972a, b), and Boyd (1990, 1992, 1993, 1994, 1998a,
b, c, 2000). The plant fossils from Upernivik Næs,
described as being part of the Atane flora by Heer (1883b),
were recognised as a separate flora (Upernivik Næs flora)
by Koch (1964) and referred to as the Upernivik flora
by Boyd (1998a, b, c, 2000).
11

Fig. 4. The first geological map of the Nuussuaq Basin published by Steenstrup (1883b). Note that only the coastal areas were known as all
travel was by boat. Steenstrup made several long journeys in an umiaq, a traditional open rowing boat of seal-skin with a crew of women.
12

Fig. 5. Plant fossils from the Atane Formation at Atanikerluk illustrated in Flora Fossilis Arctica by Heer (1883b).
13

Peak
1580 m
Peak
1722 m
Peak
1010 m
Ivissussat
Qaqqaat
Ataata
Kuua
Tupaasat
Ivisaannguit
Fig. 6. The south coast of Nuussuaq around the Ataata Kuua river delta (the large valley in the centre of the profile) which is the type area of
the Nuussuaq Group. Upper panel: Part of modern section measured by multimodel photogrammetry using oblique aerial photographs (from
A.K. Pedersen et al. 1993). Lower panel: Part of a long section painted by Harald Moltke, who accompanied K.J.V. Steenstrup on his journey
in 1898 (from Steenstrup 1900). The 33 km long profile extends a little more to the west than the map in Fig. 40. The profile shows
many of the characteristic features of the Nuussuaq Basin: Cretaceous sediments including the Atane Formation, up to 800 m (pale yellow);
Paleocene incised valleys, marine and lacustrine mudstones (grey), and hyaloclastic foreset-bedded breccias overlain by subaerial lava flows
above c. 800 m (red, blue, purple and grey, hyaloclastite breccias in pale colours, lava flows in deep colours). Outcrops of the Quikavsak Formation,
including the type section, are shown in bright yellow below the summit Point 1580 m (upper panel).
In spite of the fact that this part of Greenland had been
visited by a large number of expeditions with geological
objectives, knowledge of the marine strata was rather
poor until the Nûgssuaq Expeditions from 1938 to 1968,
probably because the marine fossils were overshadowed
by the very well-preserved plant fossils. Some marine
fossils were collected in the latter part of the 19th century
by G.F. Pfaff, C.F.V. Henriksen and Greenlanders
from Niaqornat, and important collections were made
by K.J.V. Steenstrup during his expeditions in 1871–72
and 1878–80. Additional sampling was carried out by
D. White and C. Schuchert in 1897 and by J.P.J. Ravn
and A. Heim in 1909.
Steenstrup (1874) recognised the presence of marine
strata within the Atane Formation of Nordenskiöld
(1871) along the south coast of Nuussuaq (Figs 4, 6). The
collection of marine fossils made by Steenstrup in
1871–72 in this area was examined by Schlüter (1874
pp. 30–31), who concluded that the marine strata in
West Greenland must be of Late Cretaceous age. This
conclusion was supported by de Loriol (1883) who studied
Steenstrup’s 1879 collection of marine faunas from
the north coast of Nuussuaq and from Paatuut and Ataa
on the south coast.
The collection of Scaphites from Niaqornat, which
was augmented considerably by Greenlanders who accompanied
Steenstrup on his expeditions of 1878–80, was
examined by V. Madsen (1897) who referred the dominant
species to the European Senonian Scaphites römeri
d’Orb.
In 1897, a geological expedition under the auspices
of the United States National Museum in connection with
the Peary Arctic Expedition collected fossils from the
Cretaceous and Tertiary localities on Nuussuaq. Stanton
(in: White & Schuchert 1898) was of the opinion that
the collection of marine fossils from the north coast of
Nuussuaq included a number of characteristic Late
Cretaceous types that could be equated to the Senonian
14

Peak
2010 m
Peak
1900 m Peak
1760 m
Peak
1580 m
Giesecke
Monument
Uppalluk
of Europe, but he left the possibility open that some of
the faunas from the south coast of Nuussuaq could be
Tertiary in age.
Ravn (1918) arrived at the same conclusion as Schlüter,
de Loriol and Stanton concerning the age of the marine
strata in West Greenland, namely that they are Senonian
(Late Cretaceous). His study was based on old material
stored in the Mineralogical Museum in Copenhagen and
collected by Pfaff, Henriksen and Steenstrup together
with material collected in 1909 by Ravn, and to a lesser
extent by Heim, from Disko and Nuussuaq (Heim 1910;
Ravn 1911). The work of Ravn (1918) was at that time
the most thorough study of the marine fossils and many
species were illustrated for the first time. According to
Ravn (1918 p. 330) the occurrence of American Upper
Cretaceous species in the Greenland fauna suggested that
a marine connection between West Greenland and the
central part of Canada and the United States possibly
existed in Late Cretaceous time, particularly as no affinities
with the American Coastal Plain Cretaceous fauna
or the Cretaceous of East Greenland were evident. Relying
solely on Ravn’s results, Teichert (1939 p. 155) came to
a similar conclusion, and in an accompanying map
Teichert showed the transgression of the Late Cretaceous
sea to West Greenland to be from the north-west. Frebold
(1934) described an Early Senonian fauna from East
Greenland and also made some remarks on the Senonian
fauna from West Greenland.
The pioneering stratigraphic papers by Heer (1868,
1870, 1874a, b, 1880, 1882, 1883a, b), Nordenskiöld
(1871, 1872), and Steenstrup (1883b) resulted in the
establishment of three pre-volcanic lithostratigraphic
units (the Kome, Atane and Upper Atanikerdluk
Formations) and four biostratigraphic units (the Kome,
Atane, Patoot and Upper Atanikerdluk floras). The first
geological map of the region also derives from this period
(Fig. 4; Steenstrup 1883b).
The Nûgssuaq Expeditions 1938–1968
In 1938, the Danish Nûgssuaq Expeditions ushered in
a new epoch in the study of the Cretaceous–Tertiary sediments
in West Greenland. One of the many objectives
of these expeditions was the study of the marine strata
on Nuussuaq and in other parts of the basalt region of
West Greenland (Rosenkrantz 1970) and to obtain a
more precise age for the limnic beds and their famous
floras.
In 1938 and 1939, the two Nûgssuaq Expeditions led
by A. Rosenkrantz and supported by the Carlsberg
Foundation and the Royal Greenland Trade Department
(Den Kongelige Grønlandske Handel) carried out studies
in the Nuussuaq Basin. This work was continued
after the Second World War under the auspices of the
newly established Geological Survey of Greenland
15

Fig. 7. Members of the Nûgssuaq
Expedition in 1949. Back row (from left):
Johansi, Abraham Løvstrøm, Sonja Alfred
Hansen, Andreas Tobiassen, Maggie Graff-
Petersen. Front row (from left): Alfred
Rosenkrantz, Kristian Schou, Bruno
Thomsen, Christian Poulsen, Søren Floris
and Eske Koch. Many of those in the
photo accompanied Rosenkrantz on several
expeditions. Rosenkrantz acknowledged
the assistance of the hunters from
Niaqornat, and Sonja Hansen’s discovery
of the most fossiliferous lithology when he
established the Andreas, Sonja and
Abraham Members of his Agatdal
Formation.
(Grønlands Geologiske Undersøgelse, GGU). From 1948
to 1968, 16 expeditions to the area (14 led by A.
Rosenkrantz and two by S. Floris and K. Raunsgaard
Pedersen) had to a greater or lesser degree been involved
in the study of the marine strata. A summary of the expeditions
and their results was given by Rosenkrantz (1970).
More than 47 individuals participated in the work on the
marine deposits during this 30-year period, some of
whom are seen in Fig. 7.
These expeditions represented the first attempt to
study systematically the marine Cretaceous–Tertiary sediments
in West Greenland. A new biostratigraphy was
erected (Rosenkrantz 1970 fig. 2) and it is thanks to the
efforts of the members of the Nûgssuaq Expeditions that
large collections of marine fossils were brought back to
the Geological Museum in Copenhagen. The fossils from
these outstanding collections have since been described
by many other workers:
Ammonites and belemnites: Birkelund (1956, 1965)
Corals: Floris (1967, 1972)
Coccoliths: Perch-Nielsen (1973), Jürgensen & Mikkelsen
(1974)
Crustaceans: Collins & Wienberg Rasmussen (1992)
Fish: Bendix-Almgreen (1969)
Foraminifera: H.J. Hansen (1970)
Gastropods and bivalves: Yen (1958), Kollmann & Peel
(1983), Petersen & Vedelsby (2000)
Leaves and fruits: Koch (1959, 1963, 1964)
Ostracods: Szczechura (1971)
Palynomorphs: K.R. Pedersen (1968)
Wood: Mathiesen (1961)
The gastropods were the subject of special study by
Rosenkrantz, but at the time of his death in 1974 only
a fraction of the material had been published. A catalogue
comprising the gastropod material left unpublished at
Rosenkrantz’s death was published by Kollmann & Peel
(1983) and represents the culmination of many years of
work by Rosenkrantz and the technicians and artists
under his direction. A catalogue of 115 bivalve taxa from
the Rosenkrantz collection has been published by Petersen
& Vedelsby (2000). The gastropod family Psedolividae
has been revised by Pacaud & Schnetler (1999). However,
large parts of the collection including echinoderms, serpulids,
bryozoans, nautiloids, cirripeds, brachiopods and
insects are still unpublished.
Aspects of the stratigraphy of the Cretaceous–Tertiary
sediments in the Disko – Nuussuaq – Svartenhuk Halvø
area were published in a number of papers between 1959
and 1976, in particular by Koch (1959, 1963, 1964),
Koch & Pedersen (1960), Rosenkrantz & Pulvertaft
(1969), H.J. Hansen (1970), Rosenkrantz (1970) and
Henderson et al. (1976). Some elements of the strati graphy
presented in these papers are well established, especially
the biostratigraphy of the marine Cretaceous based on
ammonites collected in situ (Birkelund 1965) and the
lithostratigraphy of the non-marine Paleocene in southern
Nuussuaq (Koch 1959). However, other stratigraphic
interpretations were based on very general descriptions
and a number of undocumented statements and correlations.
A shortcoming of the work on the sediments
during the Nûgssuaq Expeditions was the lack of a formal
correlative, regional framework for the marine and
non-marine Cretaceous strata.
16

A lithostratigraphy for the marine Danian beds of
northern and central Nuussuaq was established by
Rosenkrantz (in: Koch 1963) and Rosenkrantz (1970).
The Paleocene Kangilia and the Agatdal Formations were
subdivided into members by Rosenkrantz (1970), but
these subdivisions are not entirely satisfactory, and
Rosenkrantz’s correlation of the marine Paleocene across
Nuussuaq at member level was not documented.
As regards the marine Cretaceous, the situation was
rather better thanks largely to the comprehensive work
of Birkelund (1965). She demonstrated that the marine
Cretaceous spanned the upper Turonian – Maastrichtian
interval, and that the oldest marine strata are to be found
on Svartenhuk Halvø.
Two map sheets in GGU’s 1:500 000 map series covering
the central part of West Greenland were compiled
during this period (A. Escher 1971; J.C. Escher 1985).
The early hydrocarbon and coal-related
studies 1968–1982
In the late 1960s, the hydrocarbon potential of the basins
offshore Labrador and West Greenland was recognised.
In the early 1970s, petroleum exploration started with
the acquisition of a large number of seismic surveys and
culminated with the drilling of five exploration wells offshore
West Greenland in 1976 and 1977 (Fig. 1; Rolle
1985). In acknowledgement of the need for geological
information, GGU and the petroleum industry studied
the sedimentology, biostratigraphy and organic geochemistry
of the onshore Cretaceous–Tertiary successions.
However, these studies came to an abrupt end
when all five wells drilled offshore were declared to be
dry and the industry left West Greenland. The most
important results of these studies were published by
Henderson (1969, 1973, 1976), Sharma (1973), Elder
(1975), Schiener (1975, 1976), J.M. Hansen (1976),
Henderson et al. (1976, 1981), Schiener & Floris (1977)
and Schiener & Leythaeuser (1978).
During this phase of the work, the first overall facies
pattern was established and a palaeogeographic reconstruction
for the mid-Cretaceous was presented (Schiener
1975, 1977), but neither a basin model nor systematic
biostratigraphy or lithostratigraphy were published,
despite the great efforts of both GGU and the petroleum
industry. However, unpublished reports by Ehman
et al. (1976), Croxton (1976, 1978a, b) and Ehman
(1977) and an unpublished thesis by J.M. Hansen (1980b)
presented new stratigraphic divisions and correlations
based on palynology. The reports of Ehman et al. and
Croxton dealt with the entire sedimentary succession of
the region, but only in rather general terms. In contrast,
J.M. Hansen focussed on the marine Paleocene and presented
a more detailed stratigraphic analysis. A sedimentological
paper on the Lower Cretaceous fluviodeltaic
sediments at Kuuk, on the north coast of Nuussuaq was
published by Pulvertaft (1979). Three 1:100 000 map
sheets were compiled during this period (Rosenkrantz et
al. 1974, 1976; Pulvertaft 1987).
The first seismic lines in the Nuussuaq Basin were
also acquired during this period (Sharma 1973; Elder
1975). According to the interpretations of these authors,
the thickest succession of sediments is found along the
north coast of Nuussuaq, where it amounts to 4 km, of
which 3 km are below sea level. Along southern Nuussuaq,
the total thickness of sediments was estimated to be about
3 km, of which 2 km were interpreted to occur below
sea level.
Following the abandonment of the coal mine at
Qullissat on the north-east coast of Disko in 1972, a
major study on the coals on Nuussuaq was initiated by
GGU in 1978 with support from the Danish Ministry
of Commerce. The aim of the project was to produce
detailed geological and technical information on the
coal-bearing strata on the south coast of Nuussuaq, requisite
information for a decision whether or not to invest
in detailed exploration programmes (Shekhar et al. 1982).
Three stratigraphic boreholes were drilled and a total of
828 m of core was taken. More than 12 km of outcrop
section was measured and numerous coal samples were
analysed. Unfortunately, the results were disappointing
and did not warrant further investigation; the results
were never considered in more detail and were only documented
in an internal project report (Shekhar et al.
1982). Although the study provided a lot of new information
on the coals and the sedimentary succession, this
information was never synthesised.
Recent investigations
In the 1980s, petroleum geological research at GGU was
focussed on North and East Greenland and only limited
research was carried out in the Nuussuaq Basin, mainly
by geologists from the universities of Copenhagen and
Aarhus (Johannessen & Nielsen 1982; G.K. Pedersen
1989; Boyd 1990, 1992, 1993, 1994, 1998a, b, c, 2000).
It was not until the start of GGU’s Disko Bugt Expeditions
(1988–1992; Fig. 8) that extensive studies of the
Cretaceous–Tertiary sedimentary and volcanic succession
of the Nuussuaq Basin were initiated together with
17

Fig. 8. Members of the Disko Bugt
Expeditions in 1992. Studies on the
sediments of the Nuussuaq Basin were
carried out from a base in Uummannaq.
Participants (left to right): Ib Olsen, Søren
Saxtorph, Gregers Dam, Eskild Schack
Pedersen, Helle H. Midtgaard, Christian J.
Bjerrum, Lotte Melchior Larsen, Asger Ken
Pedersen, Stig Schack Pedersen, Martin
Sønderholm, Christian Schack Pedersen,
Gunver Krarup Pedersen and Flemming
Getreuer Christiansen.
studies on the adjacent Precambrian terrain and studies
relevant for mineral exploration in the region (Kalsbeek
& Christiansen 1992, and references therein).
During the first years of the Disko Bugt Expeditions,
most of the research on sediments dealt with the mid-
Cretaceous deltaic deposits of the Atane Formation and
the synvolcanic lacustrine deposits. It was carried out
mainly by the University of Copenhagen and resulted in
a number of case studies on sedimentology and palynostratigraphy
(see below).
The introduction of multimodel photogrammetry
during this period (A.K. Pedersen & Dueholm 1992) permitted
detailed mapping of individual rock units (e.g.
A.K. Pedersen et al. 1993, 2002). This provided a framework
for later correlation of the synvolcanic sediments
and interpretation of their palaeogeography (e.g. A.K.
Pedersen et al. 1996; G.K. Pedersen et al. 1998).
From the onset of field studies in the 1960s and the
subsequent drilling of the five dry exploration wells in
the mid-1970s, the lack of documented oil-prone source
rocks in West Greenland had been acknowledged as the
main risk in relation to oil exploration in West Greenland.
In order to confront this problem, GGU initiated a reevaluation
of the hydrocarbon potential. A systematic
analysis of the Nuussuaq Basin was initiated in 1990 as
part of the Disko Bugt Expeditions including sedimentological,
palynostratigraphical, source rock and diagenetic
studies.
At the same time, GGU reassessed some of the seismic
data acquired during the early 1970s offshore West
Greenland, and it became evident that sedimentary basins
which could contain oil and gas were much more extensive
than had previously been supposed (Chalmers 1989,
1993). This was further substantiated when seismic traverses
across the Labrador Sea acquired in 1977 by
Bundesanstalt für Geowissenschaften und Rohstoffe
(BGR) were reprocessed and reinterpreted; from the
reprocessed lines it could be seen that the continent–ocean
boundary lies much farther from the Greenland coast than
previously supposed, opening up the possibility that
prospective sedimentary basins exist in the deeper parts
of Greenland waters (Chalmers 1991; Chalmers et al.
1993). This resulted in government-funded acquisition
of more than 6000 km of seismic data by GGU in
1990–92 and a speculative survey of nearly 2000 km in
1992, all in offshore West Greenland. In addition, more
than 4000 km of seismic data in Melville Bay offshore
North-West Greenland were acquired by the industry in
1992. A licensing round was announced in West
Greenland in 1993, but no applications were submitted,
mainly due to the lack of a documented oil-prone source
rock in West Greenland.
The perception of the prospectivity of the area was
significantly enhanced, however, by the discovery of bitumen
in vugs in basalts near the base of the lava pile in
1992 and in a slim-core well (Marraat-1) in 1993 (Chri -
stiansen & Pulvertaft 1994; Dam & Christiansen 1994).
Then, in 1994, a 13 km long reflection seismic line
acquired on the southern shore of Nuussuaq revealed
that the base of the sedimentary basin is at least 5 km
below sea level at this locality (Christiansen et al. 1995).
With these results, attention began to focus on the petroleum
potential of the Nuussuaq Basin itself. After the original
discoveries, oils and bitumen were found in surface
outcrops over a wide area of western Nuussuaq and also
on the north side of Disko and on the south-eastern corner
of Svartenhuk Halvø (Christiansen et al. 1998).
Inspired by the early finds, grønArctic Energy Inc., a small
18

to provide further funding for studies to overcome the
disappointing outcome of the 1992 licensing round.
More field work was carried out on Disko, Nuussuaq and
Svartenhuk Halvø in the period between 1994 and 2002.
During the summer of 1995, the Survey acquired more
than 3700 km of seismic and gravity data, mainly in the
fjords and sounds around Disko and Nuussuaq (Chri -
stiansen et al. 1996a), and a 1200 m deep stratigraphic
slim-core hole (Umiivik-1) was drilled on Svartenhuk
Halvø in 1995 (Bate & Christiansen 1996). Additional
information was obtained using seismic and magnetic data
from the 1970s combined with an aeromagnetic survey
flown over the area in 1997 (Rasmussen et al. 2001).
The most important results from these studies include:
Fig. 9. The GRO#3 exploration well on western Nuussuaq drilled
by the Canadian company grønArctic Inc. in 1996. For location, see
Fig. 65; the drilled succession is shown in Fig. 67. Photo: Kim Zinck-
Jørgensen.
Canadian company, held a concession in western Nuus -
suaq from 1994 to 1998. During this period, the company
drilled four slim-core wells (GANW#1, GANE#1,
GANK#1 and GANT#1) and one conventional exploration
well (GRO#3) to a depth of 2996 m (Fig. 9). The
wells were drilled in areas where geological information
on the sediments beneath the volcanic rocks was completely
lacking, and they provided a large volume of new
data that also tied the outcrop areas together. Detailed
sedimentological, organic geochemical and palynostratigraphical
analyses of the wells were carried out by
the Survey and were published in numerous reports of
the ‘Danmarks og Grønlands Geologiske Undersøgelse
Rapport’ series in 1996–97. Many of the results have
later been incorporated into and summarised in other publications.
The positive results from the years 1990–1994 encouraged
the Government of Greenland and the Danish State
1) Interpretation of seismic and magnetic data, forward
modelling of gravity profiles and a reappraisal of all
available data on faults in the onshore areas (Chalmers
et al. 1999).
2) Documentation of several oil types in surface oil seeps
and wells and several possible source rock intervals
and their possible correlation with Cenomanian–
Turonian oils from the Central Western Interior Seaway
in North America, or to Upper Jurassic-sourced oils
from the Jeanne d’Arc Basin offshore Newfoundland
and in the North Sea (Bojesen-Koefoed et al. 1999,
2004, 2007; Christiansen et al. 2002).
3) Documentation of wet gas in the Umiivik-1 well (Fig.
73), suggesting the presence of a good, but overmature,
Turonian source rock for condensate or oil (Dam
et al. 1998b).
4) Establishment of a new biostratigraphic scheme for the
Cretaceous and Paleocene onshore and offshore deposits
(Nøhr-Hansen 1996; Nøhr-Hansen et al. 2002; Søn -
derholm et al. 2003).
5) Documentation of promising reservoir intervals in
the turbidite succession and a quantitative log-interpretation
of the upper part of the GRO#3 well (which
was not tested prior to casing), suggesting high hydrocarbon
saturations in sandstone units (Kristensen &
Dam 1997; Dam et al. 1998d; Kierkegaard 1998).
6) Completion of the geological mapping of eastern
Disko and south-east Nuussuaq (A.K. Pedersen et al.
2000, 2001, 2007a, b). Extensive photogrammetrical
work forms the basis of five geological profiles through
the Nuussuaq Basin (1:20 000). These profiles document
the sediments of the Nuussuaq Group and the
overlying West Greenland Basalt Group, including
the relationships between the early volcanic rocks and
the synvolcanic sediments (A.K. Pedersen et al. 1993,
2002, 2003, 2005, 2006a, b).
19

The onshore studies carried out since 1988 have
resulted in numerous publications, as summarised below:
Biostratigraphy and palaeontology:
Boyd (1990, 1992, 1993, 1994, 1998a, b, c, 2000),
Hjortkjær (1991), Piasecki et al. (1992), Koppelhus
& Pedersen (1993), Nøhr-Hansen (1993, 1996, 1997a,
b, c), Nøhr-Hansen & Dam (1997), Dam et al. (1998b,
c), Kennedy et al. (1999), Lanstorp (1999), Nøhr-
Hansen & Sheldon (2000), Nøhr-Hansen et al. (2002),
Sønderholm et al. (2003), G.K. Pedersen & Bromley
(2006).
Diagenesis:
Preuss (1996), Stilling (1996), Kierkegaard (1998).
Organic geochemistry:
Christiansen et al. (1996b, 1998, 1999, 2000), Bojesen-
Koefoed et al. (1997, 1999, 2001, 2004, 2007), Nytoft
et al. (2000), G.K. Pedersen et al. (2006).
Olsen (1991), Olsen & Pedersen (1991), G.K. Pedersen
& Pulvertaft (1992), Dueholm & Olsen (1993), Olsen
(1993), Dam & Sønderholm (1994), A.K. Pedersen
et al. (1996), Midtgaard (1996a, b), Dam & Sønder -
holm (1998), G.K. Pedersen et al. (1998), Dam et al.
(1998a, 2000), Jensen (2000), Dam & Nøhr-Hansen
(2001), Dam (2002), Nielsen (2003).
Structural geology:
Chalmers et al. (1999), J.G. Larsen & Pulvertaft (2000),
Chalmers & Pulvertaft (2001), Marcussen et al. (2002),
Bonow (2005), Japsen et al. (2005, 2006, 2009),
Wilson et al. (2006), Bonow et al. (2006a, b, 2007).
Well descriptions:
Dam & Christiansen (1994), Christiansen et al. (1994a,
1996c, 1997), Bate & Christiansen (1996), Dam
(1996a, b, c, 1997), Dahl et al. (1997), Kristensen &
Dam (1997), Nøhr-Hansen (1997a, b, c), Kierkegaard
(1998), Ambirk (2000), Madsen (2000).
Sedimentology:
G.K. Pedersen & Jeppesen (1988), G.K. Pedersen
(1989), Pulvertaft (1989a, b), Midtgaard (1991),
20

DGR
Geological setting
As a result of the opening of the Labrador Sea in Late
Mesozoic to Early Cenozoic times, a complex of linked
rift basins stretching from the Labrador Sea to northern
Baffin Bay developed along West Greenland (Fig. 1;
Chalmers & Pulvertaft 2001).
Two main episodes of regional rifting and basin development
during this time have been documented in the
area: an episode of Early Cretaceous rifting, and a Late
Cretaceous – Early Paleocene rift episode prior to the start
of sea-floor spreading in mid-Paleocene time (Dam &
Sønderholm 1998; Dam et al. 2000; Chalmers &
Pulvertaft 2001; Dam 2002; Sørensen 2006).
The most extensive outcrops of Mesozoic–Palaeogene
rocks in the entire Labrador Sea – Davis Strait – Baffin
Bay region are those of the Nuussuaq Basin in the Disko
– Nuussuaq – Svartenhuk Halvø area in central West
Greenland. This basin may be a southern extension of
the basin complex in the Melville Bay region (Fig. 1;
Whittaker et al. 1997); the offshore area between 68° and
73°N is, however, covered by Palaeogene basalts and little
is therefore known about the deeper-lying successions
in this region. A small outcrop is known from Cape
Dyer, eastern Baffin Island (Burden & Langille 1990) and
outcrops of Cretaceous–Palaeogene sediments are also seen
farther north in Arctic Canada on Bylot Island (Miall et
al. 1980; Miall 1986; Harrison et al. 1999) and on
Ellesmere Island (Núñez-Betelu 1994, Núñez-Betelu et
al. 1994a, b; Harrison et al. 1999).
During the Early Paleocene (Danian), the area offshore
southern West Greenland was subjected to major
uplift and erosion (Bonow et al. 2007). Sedimentation
resumed in the Late Danian contemporaneously with
the major episode of Paleocene volcanism in the
Disko–Nuussuaq area and continued into the Holocene
with a major hiatus spanning the Oligocene in the north
and the mid-Eocene to mid-Miocene in the south
(Dalhoff et al. 2003).
56°W
72°N
71°N
70°N
69°N
Svartenhuk
Halvø
Hareøen
Nordfjord
Mellemfjord
50 km
Ubekendt
Ejland
Uummannaq
Fjord
Itilli fault zone
Disko
KQ
Qeqertarsuaq
Vaigat
53°W
Upernivik
Ø
Aasiaat
Uummannaq
Nuussuaq
Disko Bugt
51°W
Inland Ice
Ilulissat
Grønne
Ejland
55°W 51°W
Palaeogene intrusive
complex
?
Ik
Qeqertarsuaq
?
72°N
71°N
Extensional fault
Fig. 10. Simplified geological map of the Nuussuaq Basin (after
Chalmers et al. 1999). Ik, Ikorfat fault zone; KQ, Kuu -
gannguaq–Qunnilik Fault; DGR, Disko Gneiss Ridge. The
offshore geology is indicated by paler shades.
Lower Palaeogene basalts
Maastrichtian–Paleocene
sediments
Albian–Campanian
sediments
Precambrian basement
Pre-volcanic fault
Fault with lateral
or alternating
displacements
21

Sea-level curve,
relative to present
Ma
55.8
Eoc
Ypresian
2
Kanisut Mb
58.7
61.1
65.5
Palaeogene
Paleocene
Thanetian
Selandian
Danian
Maastrichtian
Eqalulik Fm
Kangilia
Fm
1
Agatdal
Fm
Kangilia
Fm
Ifsorisoq Mb
Maligât Fm
Vaigat Fm
70.6
83.5
85.8
88.6
Cretaceous
Upper
Campanian
Santonian
Coniacian
Turonian
Itilli Fm
Umiivik Mb
Slope
Itilli Fm
Anariartorfik Mb
Fault-controlled slope
93.6
Cenomanian
undated
sediments
99.6
Lower
Albian
Kuugannguaq–Qunnilik Fault
112.0
Lavas
Hyaloclastites
Deep marine sandstones
and conglomerates
Fluviatile and deltaic sandstones
and conglomerates
Deep marine thinly interbedded
sandstones and mudstones
Mudstone
Coal
Chaotic beds
Turbidite channels
Unconformity associated with
submarine canyon incision
Unconformity associated with
valley incision
Unconformity
Tectonic phase
Uplift
Igneous activity
22

TSS
8
Agatdal
Fm Eqalulik Fm
Kangilia
Fm
Itilli Fm
Aaffarsuaq Mb
Atane Fm
Qilakitsoq Mb
Deltaic Slope
West Greenland Basalt Group
3 4 5 8
?
?
8
Quikavsak
Fm
Kangilia
Fm
Atane Fm
Qilakitsoq Mb
Deltaic
Tupaasat valley
Paatuutkløften valley
Quikavsak Fm
Atane Fm
Kingittoq Mb
Deltaic
Atanikerluk Fm
Itilli Fm
Kussinerujuk Mb
Atane Fm
Kingittoq Mb
6
?
Deltaic
Slibestensfjeldet
Fm
Atane Fm
Ravn Kløft Mb
Kome Fm
7
Basement Alluvial / lacustrine / deltaic
Kangilia
Fm
Itilli Fm
Umiivik Mb
undated
sediments
Upernivik Næs Fm
?
?
?
Basement
Estuarine ? Distal submarine lobes
7
6
5
4
3
2
1
Drift
Syn-rift
Post-rift
Syn-rift
1
2
6
7
3
4
5
Fig. 11. Tectonic events and regional depositional units, based on Dam & Nøhr-
Hansen (2001). TSS, tectonostratigraphic sequences; Eoc, Eocene. 1: GANT#1
well; 2: GRO#3 well and Itilli valley area; 3: Agatdalen; 4: Ataata Kuua and
Paatuut; 5: Atanikerluk; 6: Kussinerujuk; 7: Slibestensfjeldet; 8: Umiivik-1 well
and Itsaku. The chronostratigraphy and the sea-level curve were produced using
TSCreator PRO v. 4.0.2 (2009; http://tscreator.org). Compare with Fig. 16. See
text for further explanation.
23

The Cretaceous–Paleocene sedimentary succession of
the Nuussuaq Basin onshore West Greenland is best
known from eastern Disko and Nuussuaq, with minor,
and less well-known, outcrops in the northern part of
the region on Upernivik Ø, Qeqertarsuaq and Svartenhuk
Halvø (Fig. 10). Seismic and other geophysical data indicate
that the Mesozoic succession is at least 6 km and
possibly up to 10 km thick in the western part of the
basin (Christiansen et al. 1995; Chalmers et al. 1999;
Marcussen et al. 2002). The eastern part appears to have
much shallower depths to basement (Chalmers et al.
1999), and this part of the basin could represent thermal
subsidence following the initial rifting episode
(Chalmers et al. 1999).
The outcrops record a complex history of rifting, subsidence
and uplift commencing with an earliest Cretaceous
(or earlier) rift episode followed by a phase of thermal
subsidence during the Cenomanian – Early Campanian
(Fig. 11). Rifting resumed in the Early Campanian and
increased in the Maastrichtian – Early Paleocene (Dam
& Sønderholm 1998; Dam et al. 2000; Dam 2002),
culminating during the Early Paleocene. The first phase
of these later rift episodes was characterised by largescale
normal faulting, whereas the later episodes were
associated with continued extension and regional uplift
(Dam & Sønderholm 1998; Dam et al. 1998a, 2000;
Chalmers et al. 1999). The late phases were accompanied
by widespread igneous activity and extrusion of a
thick succession of flood basalts (Fig. 12; A.K. Pedersen
et al. 2006a, and references therein).
The exposed part of the succession in the Nuussuaq
Basin can be divided into eight tectonostratigraphic
sequences (TSS; Fig. 11); the early rift episode includes
two sequences and the late episode six sequences. These
sequences are mainly related to tectonic events marking
discrete basin-fill phases (Dam & Nøhr-Hansen 2001).
TSS 1. The oldest sediments exposed in the Disko –
Nuussuaq Basin represent a syn-rift episode of ?Aptian–
Albian age represented by the Kome and Slibestensfjeldet
Formations (Fig. 11). This rift episode is dominated by
N–S extensional faults which, however, were also reactivated
during later stages (L.M. Larsen & Pedersen
1990; Chalmers et al. 1999). The N–S trend is expressed
particularly by the Disko Gneiss Ridge and this trend
can be followed on western Nuussuaq in the Kuugan -
nguaq–Qunnilik Fault (Figs 10, 12). The eastern boundary
fault system has an overall NNW–SSE trend but is
segmented with individual segments trending N–S or
NW–SE (Fig. 10; Rosenkrantz & Pulvertaft 1969;
Chalmers et al. 1999). The Kome Formation reflects an
environment dominated by fluvial plains and local fan
deltas amid basement highs. The Kome For mation is
overlain locally by lacustrine deposits of the
Slibestensfjeldet Formation.
TSS 2. Following the early rifting episode there was a long
period of thermal subsidence that spanned the late
Albian/Cenomanian – Turonian – earliest Campanian.
It was initiated by a major flooding surface represented
by offshore and deep marine deposits of the Itilli
Formation to the north and west and by fluvio-deltaic
and shallow marine deposits of the Atane and Upernivik
Næs Formations to the east and south. The delta fanned
out to the west and north-west from a point east of Disko
(Figs 11, 12A; G.K. Pedersen & Pulvertaft 1992). On
Nuussuaq, the transition from shallow marine and fluviodeltaic
deposition in the eastern part of the basin into
deep marine deposition farther west was controlled by
the N–S-trending Kuugannguaq–Qunnilik Fault that
crosses Disko and Nuussuaq (Figs 10, 11, 12A). On
Svartenhuk Halvø contemporaneous deep-water deposition
in a slope setting is recorded by a thick distal turbidite
succession assigned to the Itilli Formation (Dam
1997). This unit includes marine anoxic shales of presumed
Cenomanian–Turonian age, that are possibly the
source for the marine Itilli oil type (Dam et al. 1998b;
Bojesen-Koefoed et al. 1999).
TSS 3. In earliest Campanian time a new tectonic episode
was initiated that lasted from the Early Campanian to
the Paleocene (Dam et al. 2000). The early phase of this
rifting episode (TSS 3) is represented by the Aaffarsuaq
Member of the Itilli Formation and lasted into the
Maastrichtian. This phase is characterised by normal
faulting, subsidence and syn-rift sedimentation. It resulted
in the development of an angular unconformity, and
deltaic deposition gave way to catastrophic deposition
in a footwall fan setting along N–S-trending normal
faults. In the eastern part of the region, uplift resulted
in significant erosion of previously deposited Atane
Formation deposits, and it is therefore expected that turbidite
sandstone bodies of regional extent are present in
the deep-water facies in the offshore basins to the west.
Facing page:
Fig. 12. Palaeogeographic reconstructions of the Nuussuaq Basin
during A: the Cenomanian/Turonian – earliest Campanian (TSS
2); B: the latest Maastrichtian (TSS 4); C: the Danian (TSS 5); D:
the earliest Selandian; E: early Selandian volcanism, and F: early
Selandian dammed lake phase. See text for further explanation.
24

A
Svartenhuk
Halvø
50 km
B
Hinterland
Delta
Slope
Nuussuaq
Basin floor
Disko
Volcanoes
Lavas
Fault
C
D
E
F
25

TSS 4–6. In late Maastrichtian – early Paleocene times,
the stress system in the region changed and extension took
place along NW–SE- and N–S-trending faults. These
form the present eastern limit of the basin and displaced
and rotated the major N–S-trending blocks in the basin
(e.g. Chalmers et al. 1999). This trend is identical to several
shear zones in the Precambrian basement east of
Disko Bugt, suggesting that these shear zones exerted an
influence on later faulting and the trend of a possible major
transfer fault situated in the Vaigat area (Dam 2002,
Wilson et al. 2006). Major faulting also occurred along
the NW–SE-trending faults and the rift blocks show evidence
of major erosion before being covered by upper
Maastrichtian – lower Paleocene marine sediments and
middle Paleocene volcanic rocks (e.g. Dam & Sønderholm
1998; Dam et al. 1998a). Birkelund (1965), Rosenkrantz
& Pulvertaft (1969), J.M. Hansen (1980b) and Nøhr-
Hansen (1996) noted that the Cretaceous faunas and
floras in the Nuussuaq Basin are similar to those of the
North American Interior Seaway while there is an overwhelming
European affinity in the Danian, suggesting
that an important change in palaeogeography and palaeoceanography
took place during the latest Cretaceous and
earliest Paleocene (Rosenkrantz & Pulvertaft 1969; J.M.
Hansen 1980b; Nøhr-Hansen & Dam 1997).
Three major tectonic episodes have been recognised
in the latest Maastrichtian – earliest Paleocene, each associated
with incision of valley systems and development
of submarine canyons. The first of these episodes (TSS 4)
is of latest Maastrichtian age and is represented by the
Kangilia Formation in which two major SE–NW-trending
submarine canyons have been documented from outcrops
(Figs 11, 12B). The second, earliest Paleocene
episode (TSS 5) is represented by the Tupaasat and Nuuk
Qiterleq Members of the Quikavsak Formation. It was
associated with major uplift of the basin and fluvial valley
incision into Early Paleocene fault scarps and was
characterised by catastrophic deposition (Figs 11, 12C).
The third episode (TSS 6) was associated with renewed
uplift during the Early Paleocene, and valleys were incised
into the old valley system (Paatuutkløften Member of the
Quikavsak Formation). Crossing the Kuuganng uaq–
Qunnilik Fault, the incised fluvial valleys pass westwards
into a major submarine canyon system. The sand-dominated
fill of this canyon system is referred to the marine
Agatdal Formation, named after equivalent valley-fill
sediments in central Nuussuaq. This episode was followed
by very rapid subsidence. The incised valleys were
eventually filled with transgressive estuarine and shoreface
deposits before they were blanketed by offshore tuffaceous
mudstones referred to the Eqalulik Formation (Figs 11,
12D) immediately prior to extrusion of picritic hyaloclastite
breccias of the Vaigat Formation (Figs 11, 12E).
The recurrent episodes of uplift and incision of submarine
canyons and valleys in Atane Formation deposits in
the eastern outcrop area resulted in major redistribution
of sandstones into the deep-water environments to the
west, and major turbidite sandstone bodies are thus suspected
to be regionally present.
TSS 7. Extrusion of the volcanic succession can be divided
into two phases and is related to continental break-up
in the Labrador Sea region (A.K. Pedersen et al. 2006a,
and references therein). The first phase, of Selandian to
Thanetian (late Paleocene) age, was dominated by extrusion
of olivine-rich basalts and picrites (Figs 11, 12E) and
later by more evolved, plagioclase-phyric basalts (Vaigat
and Maligât Formations of the West Greenland Basalt
Group). The first volcanism recorded in the Nuussuaq
Basin took place in a marine environment and eruption
centres were located in the westernmost part of the basin
(Fig. 12E). Thick hyaloclastite fans of the Anaanaa and
Naujánguit Members prograded towards the east (Figs
12F, 16). As the volcanic front moved eastwards, large
lakes were formed between the volcanic front to the west
and the cratonic crystalline basement to the east (Fig. 12F),
giving rise to synvolcanic lacustrine deposits (Atanikerluk
Formation).
TSS 8. During the Eocene, magmatic activity in the
Nuussuaq Basin resumed with an episode of intrusion
of dyke swarms and extrusion of basalts and sparse comendite
tuffs of the Kanísut Member. The volcanic succession
was dissected by N–S-trending faults and a new
NE–SW fault trend (the Itilli fault zone; Figs 10, 11).
The tectonic activity probably waned during Late
Palaeogene time, and during the Neogene the area was
lifted by 1–2 km to its present elevation (Chalmers 2000;
Bonow et al. 2007, and references therein; Japsen et al.
2009).
26

Nuussuaq Group
new group
History. The Nuussuaq Group comprises the pre- and synvolcanic
Cretaceous–Paleocene sediments on a number
of islands and peninsulas in West Greenland between
69° and 72°N (Fig. 10). Intrabasaltic sediments are not
included in the Nuussuaq Group but in the overlying West
Greenland Basalt Group, with the local exception of
thin, intra-volcanic wedges of sediment that demonstrably
interdigitate with prograding hyaloclastite breccias
and lavas of the lowermost West Greenland Basalt
Group. Initial investigations of the geology date back to
K.L. Giesecke, who described the area in detail around
1810 (in: Steenstrup 1910), Rink (1853, 1857) and
Nordenskiöld (1871); the latter erected three litho -
stratigraphic units for the pre-volcanic sediment, separate
from the intra-basaltic Ifsorisok Beds (Fig. 13; see
section on ‘Previous work’ above). However, these units
were not recognised by L. Koch (1929) in his exhaustive
account of the stratigraphy of Greenland. He referred
all the sediments to one formation – the Nugsuak For -
mation – but also predicted that “future investigations
will doubtlessly result in a division of the beds which I
have included in one formation, into several formations”
(L. Koch 1929 p. 258).
A more detailed lithostratigraphical scheme was developed
as a result of the work during the Nûgssuaq
Expeditions 1938–1968 (see section on ‘Previous work’
above; Rosenkrantz 1970). This was, however, rather
incomplete and included units, especially at member
level, that were not formally described (Fig. 13).
Name. After the Nuussuaq peninsula, where the most
extensive outcrops occur (Fig. 10).
Type area. The south coast of Nuussuaq, where the most
complete and best exposed sections of the Nuussuaq
Group occur, e.g. at Atanikerluk, the coastal slopes at
Paatuut, along the western slope of the Ataata Kuua river,
and in river gorges in the southern part of the Itilli val-
Nordenskiöld
1871
Sinnifiklagren*
Ifsorisoklagren*
Öfre
Atanekerdluk-lagren
Atanelagren
(N. Atanekerdluklagren)
Koch
1929
Nugsuak
Formation
Troelsen
1956
Sinnifik Fm*
Ifsorisok Fm*
Upper Atanikerdluk
Fm
Patoot Fm
Atane Fm
Rosenkrantz
1970
Agatdal Fm
Kangilia Fm
Marine Upper
Cretaceous
Henderson et al.
1976
Ifsorisok Fm*
Vaigat
Fm
Maligât Fm
Pautut Fm
Komelagren Kome Fm Kome Fm
U. Atanikerdluk
Fm
Agatdal Fm
Kangilia Fm
Marine Upper
Cretaceous
Atane Fm
Upernivik Næs Fm
Present paper
Ifsorisok Mb*
Maligât Fm
Vaigat
Atanikerluk Fm
Fm
Eqalulik Fm
Agatdal
Quikavsak
Fm
Fm
Kangilia Fm
Upernivik Næs Fm
Itilli Fm
Atane Fm
Slibestensfjeldet Fm
Kome Fm
Nuussuaq Group WGBG
* Intrabasaltic sediments
Fig. 13. Comparison of former lithostratigraphical subdivisions and the scheme used in this paper. All pre-volcanic and the earliest synvolcanic
sedimentary rocks of the Nuussuaq Basin constitute the Nuussuaq Group (new), which comprises 10 formations (new or revised). WGBG,
West Greenland Basalt Group.
27

Quikavsak
Formation
Vaigat Formation
Kangilia Formation
b
Atane Formation
Kangilia Formation
Atane Formation
d
d
d
Fig. 14. The western side of the Ataata Kuua river gorge, in the type area of the Nuussuaq Group; d, dolerite dyke, b, burnt mudstones. For
location, see Fig. 40; for scale, see Fig. 15.
South
North
700 m above sea level
600
Kangilia Formation, very poorly exposed
500
400
300
200
200 m
Quaternary cover
Intrusion
Eqalulik Formation
Kangilia Formation
Stream
Vaigat Formation
Atanikerluk Formation
Quikavsak Formation
Atane Formation
Qilakitsoq Member
Fig. 15. The western side of Ataata Kuua, in the type area of the Nuussuaq Group, illustrates two phases of incision. The marine mudstone
and turbidite sandstones of the Kangilia Formation represent a late Maastrichtian submarine canyon incised into the Santonian deltaic Atane
Formation; mudstones of the Kangilia Formation are shown in brown, sandstones and conglomerates in beige. The Danian Quikavsak
Formation represents a fluvial system incised into the Kangilia Formation. Photogrammetrically measured section, from A.K. Pedersen et al.
(2007b). Borehole GGU 247801 is located c. 600 m north of the outcrop shown here (Figs 40, 43).
28

ley (Figs 2, 40, 65). The section along the west slope of
Ataata Kuua has been measured photogrammetrically
(Figs 14, 15; A.K. Pedersen et al. 2007b).
Distribution. The Nuussuaq Group outcrops in West
Greenland between 69° and 72°N on Disko, Nuussuaq,
Upernivik Ø, Qeqertarsuaq, Itsaku and Svartenhuk Halvø
and has also been recorded in a number of shallow and
deep wells in the region (Figs 2, 16, 17). Possible Palae -
ogene sediments have previously been reported on
Angiissat, the south-easternmost island of a group of
small islands in Disko Bugt named Grønne Ejland
(Henderson et al. 1976 p. 345).
Differentiation of the Albian–Cenomanian Kome,
Upernivik Næs and Atane Formations that form the
lower part of the group can be difficult because these
formations all include marginal marine deposits that are
dominated by sandstones and have some sedimentary
facies in common. For practical purposes, the Kome
Formation is restricted to areas in northern Nuussuaq,
east of Ikorfat, where alluvial sediments are in contact
with basement. The Upernivik Næs Formation, which
occurs north of Nuussuaq, comprises marginal marine
sediments, while the fluviodeltaic Atane Formation is
restricted to the Disko–Nuussuaq area.
Thickness. Composite sections of outcrops and wells show
thicknesses of up to c. 3 km for the Nuussuaq Group (Fig.
17). In the western part of the area, seismic and magnetic
data suggest that the Mesozoic sediments are at
least 6 km and possibly as much as 10 km thick (Chri -
stiansen et al. 1995; Chalmers et al. 1999). A seismic
section across the Vaigat indicates that the non-marine
Cretaceous section is at least 2500–3000 m thick (Fig.
44; Marcussen et al. 2002).
Lithology and depositional environment. The exposed part
of the Nuussuaq Group consists entirely of siliciclastic
sediments (Figs 16, 17). A reconnaissance study of the
petrology of the Cretaceous and Paleocene sandstones
revealed varying feldspar contents and three types of
cement: carbonates, silica and Fe-hydroxides. Based on
differences in texture, Schiener (1975) suggested two
provenance areas: the Archaean crystalline basement
rocks (angular feldspar grains) and older sedimentary
rocks that have been recycled (well-rounded quartz grains).
Detrital zircon dating of the sediments indicates that
most of the Cretaceous sediments were transported from
areas with Archaean basement, whereas the Late
Cretaceous and Paleocene sediments at Itsaku on
Svartenhuk Halvø contain Proterozoic zircons, probably
derived from the Prøven Igneous Complex (Scherstén &
Sønderholm 2007). The basal Lower Cretaceous part of
the succession includes coarse-grained, syn-rift breccias
and conglomerates that onlap basement highs and are
overlain by sandstones, heteroliths and mudstones of
non-marine, mostly alluvial origin (Fig. 16). Slightly
younger braided river sandstones interbedded with
sandstones, heteroliths and mudstones deposited in tidal
estuarine and coastal plain environments crop out on
Upernivik Ø and Qeqertarsuaq and are referred to the
Upernivik Næs Formation.
On northern Nuussuaq, the Kome Formation is overlain
by lacustrine mudstones and sandstones of the
Slibestensfjeldet Formation. The Atane Formation un -
conformably overlies the Slibestensfjeldet Formation and
possibly also the Kome Formation. The Atane Formation
is dominated by coarsening-upward successions of mudstones
and sandstones deposited in a deltaic and fluvial
environment during the Albian to Santonian. Across the
Kuugannguaq–Qunnilik Fault (Fig. 10), the deltaic sed-
Next pages 32-33:
Fig. 16. Stratigraphy and depositional settings of the formations and
members of the Nuussuaq Group. The sections are located in Fig.
2 or in the detailed maps located in Fig. 2. Up., Uparuaq qusuitsut
(Svartenhuk Halvø). Formations are shown on the left hand side of
the logs and members on the right hand side. The vertical axis of
the diagram indicates the approximate age of the lithostratigraphical
units (data on ages are found in the selected numbered references
below). Compare with Fig. 17.
Stratigraphic abbreviations: A, Assoq Member (Atanikerluk Formation);
Ak, Akunneq Member (Atanikerluk Formation); An, Anaanaa
Member (Vaigat Formation); At, Atanikerluk Formation; AC,
Annertuneq Conglomerate Member (Kangilia Formation); E, Eqalulik
Formation; It, Itivnera Bed (Atane Formation); M, Maligât Formation;
N, Naujât Member (Atanikerluk Formation); Na, Naujánguit Member
(Vaigat Formation); NQ, Nuuk Qiterleq Member (Quivaksak
Formation); O, Ordlingassoq Member (Vaigat Formation); OAC,
Oyster–Ammonite Conglomerate Bed (Kangilia Formation); P,
Pingu Member (Atanikerluk Formation); Pa, Paatuutkløften Member
(Quikavsak Formation); RDM, Rinks Dal Member (Maligât
Formation); Sv, Svartenhuk Formation; Tu, Tupaasat Member
(Quikavsak Formation); U, Umiussat Member (Atanikerluk For -
mation).
References: 1, Birkelund (1965); 2, Boyd (1998 a); 3, Christiansen
et al. (1999); 4, Christiansen et al. (2000); 5, Dam & Nøhr-Hansen
(2001); 6, Dam et al. (1998b); 7, Dam et al. (1998c); 8, Dam et al.
(2000); 9, Koch (1964); 10, Koppelhus & Pedersen (1993); 11,
Lanstorp (1999); 12, J.G. Larsen & Pulvertaft (2000); 13, Nøhr-
Hansen (1996); 14, Nøhr-Hansen et al. (2002); 15, Olsen & Pedersen
(1991); 16, A.K. Pedersen (1985); 17, A.K. Pedersen et al. (2006b);
18, Piasecki et al. (1992); 19, Storey et al. (1998).
29

Svartenhuk
Halvø
Upernivik Næs,
Qeqertarsuaq
North coast
Nuussuaq
Western
Nuussuaq
Central
Nuussuaq
Thanetian
Umiivik
Itsaku
Sv
Up.
E of Ikorfat
W of Ikorfat
17
Aaffarsuaq
19 17
Paleocene
Selandian
Danian
Maastrichtian
Campanian
Kangilia
4
?
Kangilia Vaigat
Vaigat
12
E t
15
Itilli
Umiivik
1 6 1 7
Kangilia
O
Na
AC
Itilli Kangilia Agatdal
Vaigat
E
t
Anariartorfik
O
Na
An
Vaigat
E
Itilli
t
Aaffarsuaq
O
Na
It
Upper Cretaceous
Santonian
Coniacian
Itilli
Umiivik
3
14
Atane
8 13
Qilakitsoq
Turonian
1.5 km undated
deep marine
sediments
Lower Cretaceous
Cenomanian
Albian
Upernivik Næs
4 12 4 9
Contact
to
basement
Upernivik Næs
Slibestensfjeldet
Atane
Kome
2
Contact
to
basement
Kingittoq
Ravn Kløft
t
Volcanic rocks
Subaerial lava flow
Hyaloclastic breccia
Coal
Mudstone
Sandstone
Conglomerate
Macrofossils
Tuff
3
Key reference
30

Central
Nuussuaq
Agatdalen
South coast
Nuussuaq
Ataata Kuua
Paatuut
North coast
Disko
South coast
Nuussuaq
Eastern
Disko
South coast
Disko
Asuk Kingittoq
Pingu Skansen,
Atanikerluk
Assoq
Vaigat
E
t
O
Na
M
Vaigat
At
E
t
N
RDM
O
M
Vaigat
16 19
RDM
O
Na
M
At
t
17
A
U
N
RDM
M
At
17
A
U
P
Ak
RDM
M
At
A
17 18
RDM
Agatdal
Quikavsak
Pa
NQ
Tu
Quikavsak
Tu
Kangilia
13 14
OAC
Kangilia
5
Atane
Itilli
Aaffarsuaq
8 13
Qilakitsoq
Atane
Qilakitsoq
Alluvial fan
Lake
Fluvial channel
Flood plain
Delta plain
2 15 16
Itilli
Atane
Kingittoq Kussinerujuk
Atane
Kingittoq
Atane
Skansen
Atane
Skansen
Delta front
Estuary
Marine shoreface
Contact
to
basement
11
10
10
Marine shelf
Marine slope
Marine slope channel
31

Upernivik Næs
EItilli
Svartenhuk
Halvø
7
13 12 15 14
GRO#3
11 9 8
Upernivik Næs
Qeqertarsuaq
Itsaku Umiivik GANK#1 Kangilia Agatdalen
Tunoqqu
Aaffarsuaq
K
Upernivik Næs
Vaigat
Itilli
Kakilisaat
Nerutusoq
Vaigat
Agatdal
Kangilia
Anaanaa
Vaigat
E
Itilli
Kangilia
Na
Vaigat
E
Ag
K
I
Atane
O
Naujanguit
Qilakitsoq
E
Vaigat
Atane
Itilli
Ordlingassoq
Naujanguit
Qilakitsoq
500 m
Fig. 17. Simplified logs showing the distribution and thickness of the formations of the Nuussuaq Group. Members are only indicated for
the Atane Formation and for the volcanic formations. In most areas, the lower boundary of the Nuussuaq Group is not seen, and the thicknesses
indicated for the formations are therefore minimum values. Note that the marginal marine deposits (Kome, Slibestensfjeldet, Upernivik
Næs and Atane Formations) are thick on Disko, eastern Nuussuaq and northwards to Qeqertarsuaq. Deep marine deposits (Itilli, Kangilia
and Agatdal Formations) are thickest on western and northern Nuussuaq and on Svartenhuk Halvø. At localities 1, 3, 5 and 6, the mudstones
of the Atanikerluk Formation are interbedded with volcaniclastic breccias or subaqueous lava flows that have chemical compositions characteristic
of the Vaigat and Maligât Formations. Na, Naujánguit Member; O, Ordlingassoq Member; RDM, Rinks Dal Member; WGBG, West
Greenland Basalt Group. Compare with Fig. 16.
32

3
10 4
6 5 Qorlortorssuaq Slibestensfjeldet Kingittoq
Ataata Kuua Paatuut Asuk
Atanikerluk
2
Pingu
1
Skansen
Assoq
Vaigat
At
E
Q
K
Atane
Ordlingassoq
Qilakitsoq
Vaigat
At
Q
Atane
Ordlingassoq
Qilakitsoq
At
Atane Vaigat
I
Naujanguit Ordlingassoq
Kingittoq
Vaigat
E
I
Atane
O
Naujanguit
Ravn Kløft Kingittoq
Maligât
Atanikerluk
Q
Atane
Kingittoq Rinks Dal
Atane Atanikerluk Maligât
Skansen RDM
Atane Atanikerluk Maligât
Skansen RDM
Slibestensfj.
53°
72°
Maligât Formation
WGBG
Vaigat Formation
Atanikerluk Formation (At)
Eqalulik Formation (E)
Agatdal Formation (Ag)
Quikavsak Formation (Q)
Kangilia Formation (K)
Itilli Formation (I)
Kome
71°
70°
Svartenhuk
Halvø
7
15
14
13
11
Qeqertarsuaq
Upernivik
Næs
8
12
10
9
6
5
3 4
Nuussuaq
Atane Formation
Upernivik Næs Formation
Disko
2
Slibestensfjeldet Formation
Kome Formation
50 km
1
1
69°
Palaeogene volcanics
Precambrian basement
Cretaceous–Paleocene
sediments
33

iments of the Atane Formation pass westwards into
marine, fault-controlled slope deposits. These sediments
are referred to the Itilli Formation, of Cenomanian to
Maastrichtian age, and comprise mainly homogeneous
mudstones, thinly interbedded mudstones and sandstones,
and turbidite channel sandstones. In the Aaffarsuaq
valley, an angular unconformity separates the deltaic
Atane Formation from Campanian turbidite deposits of
the Itilli Formation (Dam et al. 2000).
Major uplift during the Maastrichtian resulted in incision
of underlying units; submarine canyon incision is
seen at several localities on Nuussuaq, viz. at Ataata Kuua,
at Kangilia, in Agatdalen and west of the Kuuganng -
uaq–Qunnilik Fault (Fig. 15, see Plate 3). At these localities,
the valley and canyon fill consists of successions of
homogeneous sandstones and conglomerates, in many
instances resulting from catastrophic gravity flow deposition.
Intercalated mudstones represent deposition from
turbidity currents. These deposits are referred to the
Kangilia Formation. Renewed uplift during the Danian
generated new incision and fluvial to tidal valley deposits
separated by lacustrine sediments filled the fluvial valleys.
The lacustrine deposits comprise thin coarseningupward
successions composed of mudstones and sand -
stones with in situ and drifted tree trunks. These sed i -
ments are referred to the Quikavsak Formation (Dam
2002). The pre-volcanic phase culminated with major
subsidence of the basin and deposition of sandstones
from sediment gravity flows (the Agatdal Formation).
During this period, the Disko area was characterised by
sedimentary bypass.
The next phase of Nuussuaq Group sedimentation
coincided with submarine volcanism west of Nuussuaq.
The oldest rocks of the West Greenland Basalt Group are
hyaloclastic breccias of the Vaigat Formation (Hald &
Pedersen 1975; A.K. Pedersen 1985; A.K. Pedersen et al.
1993, 1996, 2002, 2006b; G.K. Pedersen et al. 1998).
The contemporaneous siliciclastic marine sediments
com prise mudstones, thinly interbedded sandstones and
mudstones and chaotic beds. Volcaniclastic sandstones
and conglomerates deposited from turbidity currents are
common in this part of the succession. The marine syn-
Vaigat Formation
Itilli Formation
E
Atane Formation
Slibestensfjeldet Formation
Kome Formation
Precambrian
Fig.18. The sediments onlapping and overlying the basement high at Ikorfat on the north coast of Nuussuaq (view towards the south) represent
the base of the Nuussuaq Group. The basal sediments are represented by the Kome Formation overlain by the Slibestensfjeldet and
Atane Formations. The highest peak is c. 2000 m a.s.l.; for location, see Fig. 22. E, Eqalulik Formation.
34

volcanic sediments are referred to the Eqalulik Formation
from the latest Danian (Nøhr-Hansen et al. 2002). As the
Early Paleocene volcanic breccias of the Vaigat For mation
(West Greenland Basalt Group) prograded eastwards from
sources west of the present coastline, the formerly marine
basin was dammed and large lakes formed on eastern
Nuussuaq and Disko. The lakes were filled from the west
by hyaloclastite breccias while siliciclastic sedimentation
continued from the south-east. These sediments are re -
ferred to the Atanikerluk Formation and consist of shales
with thin tuff beds and fine-grained sandstones deposited
in two coarsening-upward successions.
the Nuussuaq Group span the Albian to the Upper
Danian – Selandian. Brackish-water dinocysts from sediments
onlapping the basement indicate a pre-Late Albian
age, and this is supported by the scarcity of angiosperms
Quaternary
m
30
40
FP93-3-1
Fossils. A rich flora and fauna from the group has been
described. The fauna numbers several hundred species
including bivalves, gastropods, nautiloids, ammonites,
belemnites, echinoderms, cirripeds, brachiopods, corals,
decapod crustaceans, serpulids, fish, ostracods,
foraminifera, bryozoans and insects. Fossil invertebrates
are best known from the Itilli, Kangilia and Agatdal
Formations. The rich flora comprises more than 600
species of plant leaves, wood, fruits, spores, pollen and
dinoflagellate cysts (hereafter named dinocysts). Well-preserved
plant fossils are mainly found in the Kome, Atane,
Quikavsak, Agatdalen and Atanikerluk Formations (for
summary of studies, see section on ‘Previous work’ above).
Dinocysts form the basis of biostratigraphy and correlation
in recent studies.
Atane Formation
50
60
70
80
90
Boundaries. The lower boundary of the group is only
exposed on the north coast of Nuussuaq at Kuuk, Vest -
erfjeld, Talerua and Ikorfat (Fig. 18), on the east coast
of Itsaku and on Svartenhuk Halvø where the group
overlies metamorphic basement that locally is strongly
weathered. The boundary was also penetrated in the
FP93-3-1 borehole on northern Disko where the Atane
Formation overlies a basement high (Fig. 19).
The upper boundary with the West Greenland Basalt
Group is diachronous (Hald & Pedersen 1975; A.K.
Pedersen et al. 1993). During the Paleocene, volcanic
breccias of the Vaigat Formation prograded eastwards
from offshore sources and isolated the formerly marine
basin in eastern Nuussuaq and Disko, eventually onlapping
the Precambrian basement east of the Ikorfat fault
zone (L.M. Larsen & Pedersen 1992; A.K. Pedersen et
al. 1996, 2002; G.K. Pedersen et al. 1998).
Geological age. Dating of the exposed and drilled parts
of the basin is mainly based on ammonites, corals,
foraminifera, coccoliths, spores, pollen, dinocysts and
macroflora fossils. The fossils indicate that outcrops of
Precambrian gneiss
100
110
120
130
Strongly weathered surface
vf f m c vc f m c
clay silt sand pebbles
Fig. 19. Detailed sedimentological log of the Atane Formation overlying
weathered gneiss basement in the the FP93-3-1 core in the
Kuugannguaq valley on north-west Disko. The well dips 60° and
driller’s depths are shown. The stratigraphic thickness of the Atane
Formation is c. 50 m; the sediments are not referred to a member.
For location, see Fig. 2. Depositional environments are indicated by
colours in the left column of the log (see Plate 1).
35

in the Ikorfat flora (Boyd 1998a, b, c, 2000). In the
Umiivik-1 well, the oldest dateable marine dinocysts are
of Turonian age; these were recorded 800 m above the
base of the well (Dam et al. 1998b). In the GRO#3 well,
the oldest dateable dinocysts are of Coniacian age and
were recorded 1500 m above the base (Christiansen et
al. 1999). Consequently, the deeper parts of these wells
may have penetrated successions older than Albian.
Age-specific biomarker data from oil seeps at several
outcrops of the Nuussuaq Group suggest that source
rocks of Aptian–Albian and Cenomanian–Turonian age
are present in the Nuussuaq Basin (Bojesen-Koefoed et
al. 2004, 2007).
40 Ar/ 39 Ar dating of the volcanic rocks coeval with the
upper levels of the Nuussuaq Group (the Vaigat Formation
and the Rinks Dal Member of the Maligât Formation)
indicates an age of 60.4 ± 0.5 Ma for these rocks (Storey
et al. 1998). This age has been recalculated to 60.8 ± 0.5
Ma based on recalibration of the Fish Canyon Tuff standard
(Skaarup & Pulvertaft 2007).
Correlation. The Nuussuaq Group is coeval with the Cre -
taceous Hassel and Kanguk Formations and the uppermost
Cretaceous–Oligocene Eureka Sound Group of the
Canadian Arctic Islands (e.g. Miall et al. 1980; Miall
1986; Burden & Langille 1990; Harrison et al. 1999).
It constitutes an onshore analogue to the Cretace -
ous–Paleocene basins offshore West Greenland (Rolle
1985; Chalmers & Pulvertaft 2001; Dalhoff et al. 2003;
Sørensen 2006; Gregersen et al. 2007) and to the
Cretaceous Bjarni, Markland and Cartwright Formations
offshore eastern Canada in the Davis Strait and Labrador
Sea (Balkwill et al. 1990; Government of Newfoundland
and Labrador 2000; Sønderholm et al. 2003).
Subdivision. The Nuussuaq Group is subdivided into the
Kome, Slibestensfjeldet, Upernivik Næs, Atane, Itilli,
Kangilia, Quikavsak, Agatdal, Eqalulik and Atanikerluk
Formations (Figs 13, 17).
Kome Formation
redefined formation
History. The geology of the Kuuk area was described by
Giesecke in 1811 (diary entry for 18 June; in: Steenstrup
1910). He mentioned that the coal seams provided fuel
for ‘Kolonien Omenak’, now the town of Uummannaq
(Fig. 20). A 0.7−1.3 m thick coal seam was exposed and
exploited until 1832 (Rink 1857). The Mineralogical
Museum in Copenhagen received 21 samples of “shale
with remains and imprints of different fossil plants, especially
ferns” collected near Kome (Rink 1855 p. 214). Heer
(1883b) described an Early Cretaceous fossil flora from
the north coast of Nuussuaq that he termed the Kome
flora. According to Nordenskiöld (1871), several of these
fossils had been collected by Rink and were sent to Heer
from the Mineralogical Museum in Copenhagen.
The Kome Formation was defined in the area between
Kuuk and Ikorfat by Nordenskiöld (1871 p. 1040) and
described as follows (translated by the authors): “The
Komelagren [Kome Formation] constitutes the older
part of the Cretaceous, according to Heer (1868). The
name designates a sedimentary, coal-bearing formation
exposed at various localities between Kuuk and Ikorfat
along the coast of Nuussuaq, south-west of Uummannaq.
The name originates from the outcrop which has the
most important coal bed and where Giesecke and Rink
most likely collected plant fossils. These beds [Komelag -
ren, the Kome Formation] are not restricted to Kuuk, but
are found, except where interrupted by gneiss highs,
along the entire coastal section between Kuuk and Ikorfat”
(Figs 2, 21, 22). Nordenskiöld (1871) proposed a stratigraphy
with a geographically restricted Lower Cretaceous
Kome Formation overlain by the Upper Cretaceous Atane
Formation which also covered southern Nuussuaq and
northern Disko. Gry (1940) interpreted the boundary
between the Kome and the Atane Formations as an un -
conformity.
Koch (1964) described the Kome Formation as occurring
almost continuously between Kuuk and Ikorfat,
interrupted only between Angiarsuit and Ujarattoorsuaq
where younger Upper Cretaceous deposits are downfaulted
(Figs 21, 22). He suggested that the beds that
unconformably overlie the Kome Formation on the north
coast of Nuussuaq could be equivalent to the Atane For -
mation or, alternatively, to the Upernivik Næs Formation.
Schiener (1977) did not find convincing evidence for
an unconformity within the section at Ikorfat and concluded
that the majority of the sediments were deposited
during the Early Cretaceous. He implied that the Atane
Formation is absent on northern Nuussuaq east of the
Ikorfat fault zone (Fig. 10).
In the Kuuk area, the Kome Formation was interpreted
to comprise fluviodeltaic deposits (Pulvertaft
1979) that were suggested to form part of the Atane
Formation by G.K. Pedersen & Pulvertaft (1992). In
contrast, Midtgaard (1996b) distinguished five sedimentary
units in the area between Ikorfat and Qaarsut
and the lowest of these is here assigned to the Kome
Formation.
36

Fig. 20. View from Uummannaq towards
the coal-bearing deposits of the Kome
Formation at Kuuk on the north coast of
Nuussuaq. The coal was being mined as
early as the 18th century for use in Uum -
mannaq. View foreshortened due to the
use of a telescopic lens. For location, see
Figs 2, 21.
Name. In his descriptions of the coal seams on northern
Nuussuaq that provided fuel for ‘Kolonien Omenak’
(the town of Uummannaq), Giesecke in 1811(in:
Steenstrup 1910) spelled the name either ‘Koome’ or
‘Kook’. Thalbitzer (1910) explained ‘Koome’ as casus
locativus of ‘Kook’, e.g. ‘in or at Kook’. The spelling
‘Kome’ was used by Rink (1857) and Heer (1882, 1883b).
Rink (1853 p. 175) wrote: “The settlement of Kome lies
at the mouth of the large valley Tuëparsoït [now Tua -
passuit, Fig. 21]. Between this and Sarfarfik a broad open
valley is found. This contains a small river (Kook) thus
the name of the site, where it reaches the shore” (translation
from Danish by the authors). The site is shown as
Kook, Kûk or Kuuk on newer maps (Fig. 21).
Distribution. The Kome Formation is presently known
from the coastal area on the north coast of Nuussuaq
between Kuuk and Ikorfat (Figs 21, 22). Gry (1940,
1942) briefly described sediments onlapping the basement
on Itsaku (Fig. 73) and referred these to the Kome
Formation on the basis of plant fossils from the lower
part of the sedimentary succession. These sediments were
tentatively referred to the Atane Formation by Chri -
stiansen et al. (2000) and J.G. Larsen & Pulvertaft (2000)
on the basis of sedimentological similarities. In the present
paper they are referred to the Upernivik Næs
Formation. East of Saqqaqdalen on southern Nuussuaq
(Fig. 2), outcrops of fluvial pebbly sandstones overlying
the basement are preserved in a small down-faulted area
(Pulvertaft 1989a, b) and are tentatively assigned to the
Kome Formation.
Type section. The type section is at Majorallattarfik, immediately
west of the Kuuk delta (Figs 21, 23). The base of
the type section is located at 70°38.60´N, 52°21.83´W.
Reference sections. Reference sections have been measured
at Slibestensfjeldet and Ikorfat (Midtgaard 1996b) (Fig.
22). These sections illustrate the marked lateral and stratigraphic,
lithological changes in the formation from
stacked conglomerates to coarsening-upward, fine-grained
sandstones and mudstones (Figs 24, 25).
Thickness. The thickness of the Kome Formation varies
from c. 25 m at Vesterfjeld to more than 150 m between
Talerua and Ikorfat, and 140 m at Majorallattarfik near
Kuuk (Figs 21, 22).
Lithology. The basal part of the Kome Formation overlies
and onlaps Precambrian basement at Kuuk, Talerua
and Ikorfat. The basement rocks are in places weathered
to a depth of 35 m (Heim 1910; Gry 1942; Pulvertaft
1979; Midtgaard 1996b). The uppermost part of the
basement consists almost exclusively of quartz grains
within a powdery matrix of kaolinite. The gneiss has a
greenish colour probably due to alteration of biotite to
chlorite (Heim 1910; Pulvertaft 1979). The basal sediments
are typically one of three main facies: (1) poorly
sorted sandstones, rich in kaolinite and devoid of sedimentary
structures, (2) diamictites, with blocks of vein
quartz in a sandy clay matrix, or (3) unsorted conglomerates
with poorly rounded quartz boulders and slabs of
silty mudstones (Fig. 26; Gry 1942; Schiener 1977;
Pulvertaft 1979). At Talerua (between Vesterfjeld and
37

1600
600
Ikorfat), the basal sediments are breccias with large clasts
comprising both gneiss with weathered feldspars and
carbonaceous mudstones (Fig. 25A). At Ikorfat, breccias
with angular gneiss clasts are overlain by a conglomerate
bed, a few metres thick, comprising subangular
clasts of quartz and intensely kaolinised feldspars. The
diamictites and poorly sorted conglomerates are not seen
above the basement highs. The poorly sorted, coarsegrained
deposits are overlain by thin conglomerates,
cross-bedded, locally channellised, coarse-grained sandstones,
mudstones and thin discontinuous coal beds (Fig.
25). Root horizons are frequent and the mudstones commonly
contain abundant comminuted plant debris (Fig.
25; Schiener 1977; Pulvertaft 1979; Midtgaard 1996b).
Fine-grained sandstones with wave-ripples forming coarsening-upward
successions occur in the upper part of the
formation and are common in the Ikorfat area. The topmost
bed of the Kome Formation is a bleached, crumbly
mudstone with abundant root-casts overlain by a coal bed
(Fig. 25C; Midtgaard 1996b).
2 km
Quaternary cover
Vaigat Formation
Vaigat Formation
Tunoqqu Member
Kome Formation
200
Sarfâgfik
Precambrian
70°40′
Kuutsiaq
600
400
Sarfaaffiip Kuussinersua
400
200
14
8
15
11
Ice
Sea/lake
Fault
Inferred base of
Cretaceous sediments
Abandoned settlement
Majorallattarfik
Kûk
800
Kuuk
17
15
800
1000
1200
Tuapassuit
1000
1400
52°25′
70°35′
1000
Fig. 21. Geological map of the area around
Kuuk (from Pulvertaft 1979). Majorallat -
tarfik is the type locality of the Kome
Formation. The sediments overlie weathered
basement and are well exposed. For
location, see Fig. 2.
38

In the Kuuk area, the sediments overlying the coarsegrained,
basal deposits consist of three facies associations:
A, B and C (Figs 24, 27, 28). Association A is
dominant and consists mainly of trough cross-bedded,
erosionally based sandstones in shoe-string or irregular
tabular bodies up to 5 m thick (Figs 24, 28). The sandstones
are coarse-grained, often gravelly, with angular
clasts, and is poorly sorted. It contains slightly to moderately
kaolinised feldspars and kaolinite cement.
Fragments of coalified wood and fine-grained plant debris
are common. The orientation of shoe-string bodies and
dip direction of foresets indicates transport from the
south-east. The sandstones alternate with dark laminated
silty mudstones containing much coalified plant debris,
thin lenses of lustrous, coalified, woody tissue and thin
coal seams (Fig. 24; Pulvertaft 1979). Association B consists
of distinctive coarsening-upward successions of mudstones,
cross-laminated siltstones, sandstones and locally
thin layers of gravelly sandstones (Figs 24, 27). Association
C is dominated by tabular cross-bedded, medium-grained,
moderately well-sorted subarkosic sandstones with pebble
lags of quartz or chert. Comminuted coalified plant
debris and mica are common in the sandstones. Foresets
dips are to the north-west. Cross-laminated, fine-grained
53°00’
52°45’
2 km
30
25
Ikorfat
25
Kussinikassaq
Angiarsuit
Nipitartukassaat
Ujarattoorsuup Killia
Ujarattoorsuaq
Ujarattoorsuup Kangilia
Siorartartarfik
30
D
20
B
Talerua
A
C
70°45’
J.P.J. Ravn Kløft
Slibestensfjeldet
Ikorfat
Qaqqarsui
Aarrusap
Kussinersua
Airport
28
Qaarsut
Vesterfjeld
Qaarsut Kussinersuat
Østerfjeld
Quaternary cover
Vaigat Formation
Vaigat Formation
Tunoqqu Member
Intrusion
Eqalulik Formation
Itilli Formation
Atane Formation
Kingittoq Member
Atane Formation
Ravn Kløft Member
Atane Formation
Undivided, west of Ikorfat
Slibestensfjeldet Formation
Umiivik Member
Kome Formation
Precambrian
Ice
Sea/lake
Fault
Strike and dip of strata
Fig. 22. Detailed geological map of the north coast of Nuussuaq, from Qaarsut to Ikorfat. The locations of the four sedimentological logs
(A–D) in Fig. 25 are indicated. Contour interval 200 m. Modified from Rosenkrantz et al. (1974) and Midtgaard (1996b). For location, see
Fig. 2.
39

Kome Formation
Precambrian
basement
m
110
100
90
80
70
60
50
40
30
20
10
0
clay
silt
vf f m c vc
sand
Fig. 23. Type section of the Kome Formation at Majorallattarfik,
immediately west of Kuuk, redrawn from Croxton (1978a, b). The
uppermost c. 20 m of the formation are poorly exposed and are not
shown on the log. Note that the facies illustrated in detail in Fig. 24
recur here in a thicker succession. For location, see Fig. 21; for a possible
correlation between Kuuk and Slibestensfjeldet, see Fig. 29;
for legend, see Plate 1.
sandstones overlying the medi um-grained sandstones
form a minor part of the association. Wave-generated
sedimentary structures or mud-draped foresets indicating
tidal influence have not been seen (Pulvertaft 1979).
Facies association C occurs at the top of the sections at
Kuuk and Majorallattarfik (Fig. 28; T.C.R. Pulvertaft,
personal communication 2008).
Fossils. The Kome Formation contains macrofossil plants
referred to the Kome flora (Heer 1883a). The genera in
the Kome flora were revised by K.R. Pedersen (1976). A
separate Ikorfat flora has been distinguished by Boyd
(1998a, b, c, 2000) in the Ikorfat area and is suggested
to be slightly older than or contemporaneous with the
Kome flora (Boyd 1998a, b, c, 2000).
Samples of mudstones collected by Croxton (1978a,
b, section C20) at Majorallattarfik near the top of the
section at Kuuk contain a poor assemblage of brackishwater
dinocysts, spores and pollen. Few specimens of
the dinocyst Vesperopsis nebulosa occur in the lower part,
whereas few specimens of Nyktericysta davisii and Pseudoceratium
interiorense occur in the upper part. The presence
of the spore Cicatricososporites auritus may indicate
a Middle to Late Albian age, whereas the absence of the
pollen Rugubivesiculites rugosus indicates a pre-Late Albian
age. The presence of Nyktericysta davisii may indicate a
younger age, as at other localities this species first occurs
in the overlying Ravn Kløft Member (Atane Formation).
Samples of mudstones collected by Midtgaard (1996b)
from the upper part of the Kome Formation reference
section at Slibestensfjeldet (Fig. 25C) also contain Ves -
peropsis nebulosa and common Pseudoceratium interiorense
and, in common with the Kuuk section, the pollen
Rugubivesiculites rugosus is absent.
Assemblages dominated by Pseudoceratium interiorense
are known from the Slibestensfjeldet Formation, whereas
assemblages dominated by Nyktericysta davisii first occur
in the Ravn Kløft Member of the Atane Formation
between Vesterfjeld and Ikorfat (Fig. 29). Croxton (1978a,
b) noted the absence of angiosperm pollen and the presence
of spores such as Cicatricosisporites, Gleicheniidites,
Pilosisporites and Vitreisporites, indicating an early to mid-
Cretaceous age.
Depositional environment. The diamictites and poorly
sorted conglomerates in close association with the basement
highs are interpreted as mass-flow deposits (Figs
25, 29); talus cones and alluvial fans filled the topographic
lows on the basement surface with immature
sediments (Midtgaard 1996b). The lack of mass-flow
deposits above the basement highs suggests that the ini-
40

m
m
15
14
14
13
12
11
10
9
8
7
6
5
13
12
11
10
9
8
7
6
5
Lithology and structures
Sandstone/pebbly
sandstone, structureless
Laminated sandstone
Cross-bedded sandstone
Ripple cross-laminated sandstone
Convolute lamination
Burrows
Coalified wood fragments
Coal
Laminated mudstone/siltstone
Weakly laminated mudstone
Depositional environment
4
3
4
Fluvial channel
Flood plain
Facies association A
of Pulvertaft (1979)
3
Delta front
Facies association B
2
2
1
0
mud
sand gravel
1
0
mud
sand gravel
Fig. 24. Reference section of the Kome Formation at
Kuuk. The log to the left is representative of facies association
A, while association B is seen from 3.1–9.3 m in
the log to the right (from Pulvertaft 1979). For location,
see Fig. 21; for legend, see Plate 1.
41

m
40
A B C
m
36
Slibestensfjeldet
Fm
m
38
30
30
30
Kome Formation
20
Kome Formation
20
Kome Formation
20
★
10
10
10
★
0
mud
sand
gravel
0
mud
sand
gravel
0
mud
sand
gravel
Section base 20 m above sea level (a.s.l.)
2 m a.s.l.
242 m a.s.l.
Fig.25. Reference sections of the Kome Formations illustrating abrupt facies change and numerous horizons with rootlets. A and B are from
the lower part of the formation and C and D are from the uppermost part of the formation. Sections C and D also show the overall decrease
in grain-size towards the west. The boundary between the Kome Formation and the overlying Slibestensfjeldet Formation is shown in section
C. From Midtgaard (1996b). For legend, see Plate 1; for location, see Fig. 22.
42

Kome Formation
m
40
30
20
D
tial relief was levelled out as sediments accumulated and
buried the highs. The alluvial fans were succeeded by
fan deltas representing both subaerial and subaqueous
deposition; the latter increases towards Ikorfat (Fig. 25D).
The sparse dinocyst assemblage indicates that the water
was intermittently brackish.
The coarse sandstones of facies association A at Kuuk
are interpreted as fluvial deposits. Their low textural and
mineralogical maturity together with palaeocurrent indicators
point to derivation directly from a weathered basement
to the south-east, without reworking en route, and
to rapid sedimentation. The dark mudstones are interpreted
as overbank deposits of a floodplain environment
or deposition in shallow lakes. The mudstones of facies
association B are interpreted as having been deposited
from suspension in bodies of standing water, presumably
interdistributary bays or lakes (Fig. 23, 24). Sedimentary
structures in the sandstones of facies association C suggest
deposition from a sandy braided river flowing from
the south, and the higher textural and mineralogical
maturity of the sandstones indicates more protracted
fluvial transport (Pulvertaft 1979). The palaeosol that caps
the Kome Formation represents a widespread regressive
event (Figs 25C, 30; Midtgaard 1996b).
10
0
mud
290 m a.s.l.
sand
gravel
Boundaries. The Kome Formation overlies an undulating
Precambrian gneiss topography, filling valleys or
depressions (Henderson et al. 1976; Schiener 1977;
Pulvertaft 1979; Midtgaard 1996b). The lower boundary
of the formation is exposed at Kuuk, Ikorfat and
Talerua (Figs 2, 21, 22). In the coastal cliffs of northern
Nuussuaq, the relief on the gneiss surface can be seen to
exceed 225 m (Fig. 22). At Vesterfjeld, the basement is
weathered to a depth of 30 m with a gradual downward
transition into unaltered gneiss. In western Disko
(Stordal), the Precambrian basement is exposed, locally
with a 5−10 m thick weathered cap (A.K. Pedersen &
Ulff-Møller 1980). In other exposures, the gneiss is relatively
unweathered (Schiener 1977; Midtgaard 1996b).
The lower boundary of the Kome Formation thus displays
a variety of basement−sediment transitions.
The upper boundary of the Kome Formation is a
sharp lithological boundary that varies very little laterally
(Figs 25C, 30). It is placed on top of a palaeosol
horizon and was interpreted as a sequence boundary by
Midtgaard (1996b). Previous workers, e.g. Nordenskiöld
(1871), Gry (1942) and Midtgaard (1996b), have considered
the Kome Formation to be overlain by the Atane
Formation on Nuussuaq. We propose that the new
Slibestensfjeldet Formation separates the Kome and Atane
43

Slibestensfjeldet Formation
Kome Formation
Precambrian
Fig. 26. Contact between Precambrian basement and the Kome Formation at Talerua. The sediments onlap the relief on the basement surface.
The height of the coastal cliff is c. 30 m. For location, see Fig. 22.
Formations in the area between Ikorfat and Slibe -
stensfjeldet.
Geological age. Various fossils contribute to the determination
of the geological age of the Kome Formation.
Plant macroflora suggests a Barremian to Aptian age
(Heer 1882; K.R. Pedersen 1968). The Ikorfat flora suggests
an Early to Middle Albian age (Boyd 1998a, b, c,
2000). Based on spores and pollen as well as scarce
dinocysts, Ehman et al. (1976) suggested a Late Albian
to Early Cenomanian age, whereas Croxton (1978a, b)
interpreted the sediments to be older than Middle Albian.
In this study, the spores, pollen and brackish-water
dinocysts are considered suggestive of a pre-Late Albian
age. Consequently, the Kome Formation is suggested to
be of albian age.
Correlation. It has previously been stated by Troelsen
(1956) and Rosenkrantz (1970) that the sediments
exposed on the north coast of Nuussuaq, east of the
Ikorfat fault zone, are older than the fluviodeltaic
Cretaceous sediments known from the rest of the Nuus -
Fig. 27. The type locality of the Kome
Formation at Majorallattarfik showing
outcrop of facies association B (see text for
explanation). Person for scale (circled) is
standing on delta front deposits (see also
Fig. 24, right-hand column). For location,
see Fig. 21. Photo: T.C.R. Pulvertaft.
44

Fig. 28. Reference locality of the Kome Formation at Kuuk showing
outcrop of facies associations A and C (see text for explanation,
see also Fig. 29). For location, see Fig. 21. Photo: T.C.R. Pulvertaft.
C
A
suaq Basin. However, Lanstorp (1999) suggested a Middle
to Late Albian age for the Atane Formation at Tartunaq
(south-east Nuussuaq), thereby shortening (or removing)
the time gap between the Kome and Atane Formations.
Nevertheless, the Kome Formation is retained as a discrete
lithostratigraphic unit characterised by the onlap
relationship to the basement, the coarse-grained conglomeratic
character and the significant lateral facies
changes (Fig. 25). These features indicate a depositional
environment that was markedly different from that which
produced the cyclic, aggradational Atane Formation.
In the Kuuk area, the mudstones of association B and
the sandstones of association C (Pulvertaft 1979), referred
here to the Kome Formation, may correlate laterally with
the Slibestensfjeldet and Atane Formations, respectively,
farther to the north-west (Fig. 29). Thus, the mudstones
of association B (Fig. 24) and the mudstone-dominated
unit of the type section (40–80 m in Fig. 23) are thought
to represent proximal correlatives of the Slibestensfjeldet
Formation. The sandstones of association C display an
erosional base and occur towards the top of the exposed
sections (Fig. 29). This unit contains chert pebbles, a
characteristic feature of the Atane Formation and particularly
the fluvial sandstones of the Ravn Kløft Member
of the Atane Formation (see below). It is tentatively suggested,
therefore, that the erosional base of the sandstones
in facies association C may correlate with the
erosional boundary between the Slibestensfjeldet and
Atane Formations, i.e. that the uppermost Kome
Formation in the Kuuk area correlates with the lowermost
Atane Formation to the north-west (Fig. 29).
SE
NW
Ikorfat fault zone
Vaigat Fm
Eqalulik Fm
Itilli Fm
C
Kome Fm
A
★
B
?
?
Atane Fm
Kingittoq Mb
★
★
Slibestensfjeldet Fm
Ravn Kløft Mb
Kome Fm
Kome Fm
Kuuk
Qaarsut
Pseudoceratium interiorense
Talerua
★ Nyktericysta davisii
Ikorfat
Kangilia Fm
Fig. 29. Schematic profile (scale arbitrary) along the north coast of Nuussuaq between Kuuk and Ikorfat showing correlation of the litho -
stratigraphic units. The sediment outcrops are bounded to the east by the basin boundary fault and to the west by the Ikorfat fault zone. The
occurrence of two species of dinoflagellate cysts is shown. These species are known from other localities in the Nuussuaq Basin. For location
of outcrops, see Figs 21, 22; A, B, C, facies associations discussed in the text. Pale red indicates Precambrian basement.
45

Slibestensfjeldet Formation
new formation
History. The Slibestensfjeldet Formation has previously
been described as Unit 2, an informal lithological unit
in the Slibestensfjeldet–Ikorfat area (Midtgaard 1996b).
Name. After the prominent mountain of Slibestensfjeldet
on the north coast of Nuussuaq (Fig. 22).
Distribution. The Slibestensfjeldet Formation is known
only from the north coast of Nuussuaq between Vesterfjeld
and Ikorfat (Fig. 22; Midtgaard 1996b). The formation
is not known to be preserved north of Nuussuaq, but it
is expected to continue southwards, for some distance,
in the subsurface. The extent of the formation west of
the Ikorfat fault is not known.
Type section. The type section is at Kussinikassaq where
the formation is thickest (Figs 22, 30), immediately east
of the basement high at Ikorfat beginning at an altitude
of c. 60 m a.s.l. The base of the type section is located
at 70°46.20´N, 53°03.37´W.
Reference sections. Reference sections are found at
Vesterfjeld, c. 860 m a.s.l., and in two gullies on Slibe -
stensfjeldet c. 1 km east of Talerua, beginning at an altitude
of c. 320 m a.s.l. (Fig. 30).
Thickness. The Slibestensfjeldet Formation increases in
thickness from 90 m at Vesterfjeld to c. 200 m at Kus -
sinikassaq (Figs 22, 30).
Lithology. A considerable lateral change in lithology characterises
the Slibestensfjeldet Formation from Vesterfjeld
to Ikorfat, a distance of approximately 10 km (Fig. 30;
Midtgaard 1996b). At the type section, the formation is
dominated by mudstones, interbedded with 0.2–2 m
thick sandstone beds, which are structureless, parallel
laminated, cross-laminated or hummocky cross-stratified
(Figs 30, 31, 32). The mudstones contain c. 5% carbon,
almost entirely of organic origin, traces of pyrite are
restricted to a thin coal bed, and the calculated carbon/
sulphur (C/S) ratios are c. 100. The sandstone interbeds
in the c. 200 m thick mudstone unit become increasingly
common upwards. At the top of this coarsening-upward
succession is a medium-grained sandstone unit 5 m thick,
showing steeply dipping foresets; this facies is restricted
to the areas west of the Talerua fault. In the east, the formation
is dominated by sandstones interbedded with
thin mudstones and conglomerate beds. Laminated black
mudstones with sand streaks are abruptly overlain by
very fine- to fine-grained, well-sorted sandstones dominated
by horizontal lamination and hummocky crossstratification,
whereas low-angle cross-bedding and wave
ripple cross-lamination are subordinate (Midtgaard
1996a). The sandstones are often slightly bioturbated.
Thin conglomerate beds composed of well-rounded clasts
and showing erosional bases and wave-rippled tops, recur
throughout the formation (Midtgaard 1996a).
Fossils. The mudstones contain an assemblage of brackish-water
dinocysts dominated by Pseudoceratium interiorense
whereas the pollen Rugubivesiculites rugosus is
absent (Figs 29, 30). Plant macrofossils from the lowermost
part of the formation are referred to the Ikorfat
flora, which has been assigned to the Early–Middle Albian
(Boyd 1998a, b, c, 2000).
Depositional environment. The widely distributed and
thick coal bed at the base of the Slibestensfjeldet Formation
indicates accumulation of peat under a slowly rising
ground-water table. The overlying fine-grained, wave-rippled
sandstones are interpreted as lake shoreline deposits
and indicate an increasing rate of water level rise, which
continued to the deposition of mudstones at depths
below wave-base. In the mudstones, the C/S ratios of c.
100 and the stratigraphical position between the fluvial
Kome and the fluvial Ravn Kløft Member indicate that
the Slibestensfjeldet Formation was deposited in a large
and deep lake. The overall, coarsening-upward, vertical
facies succession is interpreted to record the infill of the
lake and progradation of the shoreline. The presence of
dinocysts, which are interpreted as brackish-water forms,
suggests that the lake was connected to a coastal lagoon.
The lake increased in depth from east to west, and
wave-influenced, relatively shallow-water facies are only
known from Vesterfjeld and Slibestensfjeldet. The conglomerate
beds represent transgressive lags created by
wave erosion and winnowing. The nearshore sandstones
accu - mulated in large complex bedforms overprinted
by wave-ripples (Midtgaard 1996a). The upper part of
the Slibe stensfjeldet Formation locally developed as a
Facing page:
Fig. 30. Type section of the Slibestensfjeldet Formation at Kus sini -
kassaq; reference sections of the formation at Vesterfjeld and
Slibestensfjeldet. Note the marked increase in thickness towards the
west (Kussinikassaq). All logs are from the north coast of Nuussuaq
(Fig. 22). For legend, see Plate 1; GD, Gilbert Delta; Ps, palaeosol.
46

Vaigat Fm
Vesterfjeld
Slibestensfjeldet
Kussinikassaq
Slibestensfjeldet Formation Atane Formation
Ravn Kløft Member
Slibestensfjeldet Formation
Ravn Kløft Member
mud
GD
sand pebbles
Slibestensfjeldet Formation
Ravn Kløft Member
GD
c. 50 m not shown
m
20
10
Kome Fm
mud
Ps
sand pebbles
0
Kome Fm
mud
Ps
sand pebbles
47

Fig. 31. Mudstones with thin sandstone beds in the lower part of the Slibestensfjeldet Formation at Kussinikassaq, near Ikorfat. For location,
see Fig. 22.
Atane Formation
Ravn Kløft Member
Slibestensfjeldet Formation
Fig. 32. The upper part of the Slibestensfjeldet Formation in its type locality at Kussinikassaq, where heterolithic sandstone bodies with wavegenerated
sedimentary structures (see also Midtgaard 1996 a, b) are overlain by lower shoreface sandstones (see Fig. 30) and locally by Gilbert
delta foreset beds. The Slibestensfjeldet Formation is erosionally overlain (dashed line) by the fluvial Ravn Kløft Member of the Atane
Formation. The height of the section is c. 100 m. For location, see Fig. 22.
48

Gilbert delta in the Ikorfat area (Figs 30, 32; Midtgaard
1996b). The extent of the lake or lagoon west of Ikorfat
is not known. It may be speculated that subsidence along
the Ikorfat Fault affected the development of the lake.
Boundaries. The lower boundary of the Slibestensfjeldet
Formation is sharp and varies very little laterally; it is placed
at the base of a 20−110 cm thick, continuous coal bed
that overlies a palaeosol (Fig. 30).
The upper boundary of the Slibestensfjeldet Formation
with the Atane Formation is defined by an abrupt contact
between shoreface sandstones or Gilbert delta sandstones
and coarse-grained, pebbly fluvial sandstones of
the Ravn Kløft Member (Figs 30, 32). The boundary has
been interpreted either as a minor angular unconformity
(Gry 1940; Koch 1964) or as the conformable, yet erosional
base of a channel (Ehman et al. 1976; Schiener 1977;
Croxton 1978a, b; Midtgaard 1996b). Midtgaard (1996b)
interpreted the boundary as a sequence boundary.
Geological age. Based on plant macrofossils referred to the
Ikorfat flora, the Slibestensfjeldet Formation has been
assigned an Early to Middle Albian age (Boyd 1998a).
The dinocysts suggest a Late Albian age (Ehman et al.
1976; Croxton 1978a, b) or more likely a pre-Late Albian
age (this study).
Correlation. The Slibestensfjeldet Formation in the
Slibestensfjeldet outcrops may correlate with coarsening-upward
successions in the Kome Formation at Kuuk
(Fig. 29). Outcrops connecting these two areas are, however,
not present.
Upernivik Næs Formation
revised formation
History. The sedimentary outcrops at Upernivik Næs were
described by Steenstrup (1883b) who noted that the coalbearing
sediments have a thickness of at least 860 m. The
lithology was not considered different from the coalbearing
successions known from Nuussuaq and Disko.
The macrofossil plants collected at Upernivik Næs by
Steenstrup were referred to the Atane flora by Heer
(1883b). In contrast, Seward (1926) compared them to
the Kome flora. Koch (1964) considered the fossil flora
from Upernivik Ø as difficult to interpret due to similarities
to both the Kome and the Atane floras and suggested
that the Upernivik Ø flora could occupy an
intermediate position. Troelsen (1956) did not recognise
the Upernivik Næs Formation, which was later
described by Koch (1964).
Name. The formation is named after Upernivik Næs on
the south-western corner of the island of Upernivik Ø
(Figs 2, 33).
Distribution. The formation is known from Upernivik
Ø. The marginal marine sediments on the island of
Qeqertarsuaq and on Itsaku are here referred to the
Upernivik Næs Formation (Figs 2, 73; Ødum & Koch
1955, Christiansen et al. 2000; J.G. Larsen & Pulvertaft
2000).
Type section. The type section is located on the south-western
corner of Upernivik Ø, along a large stream that
flows out on the south coast of the island c. 2.5 km east
of Upernivik Næs (Figs 33–35). The base of the type
section is located at 71°09.88´N, 52°54.52´W.
Reference section. A reference section is exposed in a coastal
cliff on western Qeqertarsuaq (Figs 2, 36, 73).
Thickness. The formation is c. 1600 m thick at Upernivik
Næs, where the strata generally dip c. 15° towards the
north-east (Henderson & Pulvertaft 1987). Croxton
(1978b) measured a 1310 m long section (termed the
C9 section) along the southern coast of Upernivik Næs;
this section coincides with the type section in its upper
part. In the type section, the formation is exposed up to
c. 500 m a.s.l. (Fig. 33).
Lithology. The section at Upernivik Næs is dominated
by sandstones; mudstones constitute only a minor part
(Figs 34, 35). On Qeqertarsuaq, sandstone-dominated
successions are locally overlain by clast-supported conglomerates,
in which the clasts are dominantly from the
metamorphic rocks of the widely exposed Karrat Group
(Fig. 37; Henderson & Pulvertaft 1987). The formation
has been studied at a reconnaissance level by Midtgaard
(1996b), who divided the sediments of the formation into
four facies associations.
Facies association A. Coarse-grained, poorly sorted
sandstones constitute up to 34 m thick composite depositional
units (Fig. 38). Some of these are distinctly fining
upwards. Basal channel lags contain pebbles of
crystalline rocks and locally also mudstone clasts, logs and
carbonaceous debris. The sandstones are cross-bedded with
most palaeocurrent directions towards the western quadrant.
Soft-sediment deformation structures are common.
49

■■
Facies association B. Well-sorted, fine- to mediumgrained
sandstones with abundant mudstone clasts characterise
the association. Siltstone and mudstone beds
and laminae form an important component and in places
are heterolithic and ripple-cross laminated. The sandstones
are dominated by planar or trough cross-bedding
that indicates palaeocurrents to the north. Some sandstones
have mud-draped foresets and show bundled lamination
(Fig. 39). The mud-dominated heteroliths and
mudstones contain much comminuted plant debris; bioturbation
varies from moderate to intense (Fig. 39).
Facies association C. Sandstones interbedded with mudstones
constitute 3−8 m thick successions. The sandstones
range from very fine- to very coarse-grained, the
beds are erosionally based and pinch out laterally. They
are cross-laminated, cross-bedded or locally horizontally
stratified. The tops of the sandstone beds are moderately
bioturbated. The mudstones are black, fissile and sandstreaked,
and sometimes contain abundant plant debris
and vitrinite lenses. Sandstone dykes are common, and
gentle folding indicates that they were intruded before
or during compaction.
Facies association D. Coarsening-upward successions
comprising black fissile mudstones, mudstones with
sandstone lenses, mud-draped ripple cross-laminated,
fine-grained sandstones, and trough cross-bedded sandstones
with comminuted plant debris (Midtgaard 1996b).
These deposits constitute only a minor part of the section
shown in Fig. 34.
Fossils. The Upernivik Næs Formation contains angio -
sperm plants referred to the Upernivik Næs flora (or
Upernivik flora), which is interpreted as intermediate in
age between the Kome flora and the Atane flora (Koch
1964; Boyd 1998a). Macrofossil plants from Qeqertarsuaq
correspond to species known from outcrops at Upernivik
Næs and Atanikerluk (Ødum & Koch 1955). Few palynomorphs
have been recorded from Croxton’s (1978b)
C9 section through coastal exposures and the type section
at Upernivik Næs. The presence of a few specimens
of the pollen Rugubivesiculites rugosus throughout the
section indicate a Middle Albian to Turonian age, and
the co-occurrence with a few specimens of the dinocysts
Nyktericysta davisii and Quantouendinium dictyophorum
in the lower part of the section suggests correlation to
the lower part of the Atane Formation (?Ravn Kløft
Member). A large specimen of the dinocyst Nyktericysta
davisii has been recorded from the middle part of the C9
section. Similar forms are common in sediments on
Qeqertarsuaq (Christiansen et al. 2000) and from a single
fully marine sample from the Atane Formation at
Ikorfat dated as Early Turonian. The sediments in facies
20
■■ ■■ ■■ ■■
30
■■
■■ ■■
1760
1939
71°12'
Fig. 33. Geological map of Upernivik Næs
on the south-western tip of Upernivik Ø.
The type section of the Upernivik Næs
Formation is located in the ravine 2.5 km
east of Upernivik Næs. Slightly modified
from Henderson & Pulvertaft (1987). For
location, see Fig. 2. The contour interval is
200 m.
20–25
740
10
Upernivik Næs
20
18
22
16
10 15
■■ ■■
Glacier
Sea/lake
53° 2 km
Upernivik Næs Formation
with conglomerate
■■
Dolerite/basalt
71°09'
Fault (ticks on downthrow side)
Facing page:
Fig. 34. Type section of the Upernivik Næs
Formation; from Midtgaard (1996b). Notice
the presence of tidal deposits. For legend, see
Plate 1; for location, see Fig. 33.
50

150
300
450
100
250
400
m
550
50
200
350
500
?
?
0
clay
si sand gravel
clay si sand gravel
clay si sand gravel
clay si sand gravel
51

Precambrian Karrat Group
Upernivik Næs Formation
Fig. 35. Type locality of the Upernivik Næs Formation. The central peak is c. 1700 m high. For location, see Fig. 33.
association B contain trace fossils such as Skolithos, Are -
nicolites, Conichnus, Planolites, Rhizocorallium and
Pelecypodichnus (Midtgaard 1996b).
Depositional environment. The sandstones of facies association
A are interpreted to have been deposited in braided
fluvial channels. The scarcity of interbedded floodplain
or levee facies suggests that the channels were migrating
laterally. The abundant soft-sediment deformation structures
suggest synsedimentary tectonic activity.
The heterolithic, burrowed sandstones (facies association
B) are interpreted to have been deposited in an
estuarine environment – in tidal channels, tidal point bars,
tidal deltas, tidal flats, bay mudstones, and on the shoreface
as transgressive lags. The palaeocurrents are interpreted
to reflect longshore tidal transport.
The interbedded sandstones and mudstones (facies
association C) are thought to represent a coastal plain environment
and include lagoonal, mudflat and marsh
deposits, crevasse splay deposits and deposits in small
channels. The scarcity of rootlets and the presence of
trace fossils suggest brackish-water conditions. Intrusion
of the sandstone dykes may have been triggered by earthquakes.
The coarsening-upward successions (facies association
D) are interpreted as deltaic deposits. The lack of
wave-generated sedimentary structures in facies association
D in the Upernivik Ø section indicates deposition
in a low-energy environment, probably an interdistributary
bay or the inner part of an estuary, i.e. a bayhead
delta (Midtgaard 1996b). Higher-energy facies on Qe -
qertarsuaq and Itsaku suggest the influence of waves and
storms on the delta deposits (J.G. Larsen & Pulvertaft
2000).
Boundaries. The lower boundary of the Upernivik Næs
Formation is not exposed in the type section nor in the
reference section. Conglomerates with large clasts of both
weathered and fresh basement rocks have been reported
close to the boundary fault at Upernivik Næs (Fig. 33),
from a small outcrop on the north-western part of
Upernivik Ø (Henderson & Pulvertaft 1987 fig. 46),
from Qeqertarsuaq and from Itsaku (Rosenkrantz &
52

Fig. 36. Outcrop of the Upernivik Næs
Formation on Qeqertarsuaq; for location,
see Fig. 73. Reddish-brown intrusions
cross-cut (right) and cap the sediments.
Pulvertaft 1969). The boundary between the Kome and
the Upernivik Næs Formations is at present not known.
The upper boundary of the formation is an erosional
contact with the Kangilia Formation on Itsaku and with
Quaternary deposits on Upernivik Næs and Qeqertarsuaq.
Geological age. The Upernivik Næs flora contains angio -
sperm plants, which suggests a greater similarity to the
Atane flora than to the Kome flora (Koch 1964). Koch
recommended, however, that until the Cretaceous floras
are thoroughly revised, the Upernivik Næs flora should
Fig. 37. Clast-supported conglomerate of the Upernivik Næs Formation on Qeqertarsuaq. Hammer for scale; for location, see Fig. 73.
53

Fig. 38. Channellised sandstones of the Upernivik Næs Formation in the lower part of the type section. Thickness of sandstone unit is approximately
10 m. For location, see Fig. 33.
be eliminated from the discussion of the age of the Kome
and Atane Formations and treated as an independent
problem (Koch 1964 p. 540).
Rosenkrantz (1970) suggested that the Upernivik Næs
flora is of Albian−Turonian age. Boyd (1998a) suggested
that the Upernivik Næs flora is contemporaneous with
his Ravn Kløft flora which he referred to the Middle–Late
Albian and earliest Cenomanian. The poor palynological
assemblage indicates a Late Albian to Early Turonian
age (Croxton 1978a, b; this study).
Fig. 39. Detail of tidally influenced
deposits of the Upernivik Næs Formation
in the lower part of the type section.
Person for scale; for location, see Fig. 33.
54

Correlation. The Upernivik Næs flora was suggested to
be coeval with the Ravn Kløft flora by Boyd (1998a). This
suggests a correlation between the Upernivik Næs
Formation and the Ravn Kløft Member of the Atane
Formation (Figs 13, 16).
Atane Formation
redefined formation
History. Nordenskiöld (1871) erected the Atane Formation
(Atanelagren), naming it after the now-abandoned settlement
of Atane (now Ataa, Figs 3, 40). He described
the unit to be more shaly than both the underlying Kome
Formation and the overlying Upper Atanikerdluk For -
mation, and interpreted the Atane Formation as freshwater
deposits. He referred the formation to the Upper
Cretaceous, following Heer (1868), with a distribution
on southern Nuussuaq (between Atanikerluk and Ataa),
northern Disko (at Qullissat) and at Kuuk on northern
Nuussuaq (at altitudes above 250–300 m). Outcrops
with coal seams were visited by Steenstrup (1874), who
noted the occurrence of marine invertebrates in mud stones
between the coal seams at Paatuut and Nuuk Qiterleq.
The Atane Formation normally appears as a striped
white, grey and black sandy and shaly unit rich in coalified
plant fossils (Fig. 41) that formed the basis of the
classic studies by Heer (1868, 1870, 1874a, b, 1880,
1883a, b). However, self-combustion of the mudstones
has locally produced brick-red, hard and fissile burnt
slabs (Fig. 42) in which fossils are excellently preserved
as impressions. Burnt mudstones are fairly common in
the Paatuut (formerly spelled Patoot, Pâtût or Pautût) and
Kingittoq areas, and they were included in the regional
collection that Steenstrup sent to O. Heer (Steenstrup
1883a, b). Based on their colour, Heer treated the samples
of burnt mudstones from Paatuut as lithostratigraphically
different from those containing the Atane
flora. Thereby a Patoot Formation (i.e. the sediments
comprising the Patoot flora) was introduced and subsequently
treated as a formal unit (Troelsen 1956).
Steenstrup (1883c) objected to Heer’s interpretation of
a stratigraphic boundary between the unburnt and the
burnt mudstones from Paatuut since he had observed that
the burnt mudstones are laterally equivalent to the normal,
unburnt sediments.
Steenstrup (1883a) suggested that all the Cretaceous
sediments from Svartenhuk Halvø to Disko should be
enclosed in one lithostratigraphic unit. He envisaged the
depositional environment of the horizontally bedded
mudstones and sandstones as shallow marine on account
of his collections of invertebrates (bivalves and echinoids),
although the well-preserved plant remains indicated
deposition close to vegetated areas (Steenstrup
1883a p. 48).
The Early Cretaceous to Miocene age proposed by
Heer for the coal-bearing deposits in West Greenland
was discussed by A. Heim and J.P.J. Ravn, who both suggested
that Heer’s interpretation spans too long a period.
Instead they interpreted all the sediments as Upper
Cretaceous to Eocene (Heim 1910), more specifically the
Kome flora as Albian, the Atane flora as Cenomanian,
the Patoot flora as Senonian and the Atanikerdluk flora
as Eocene (Ravn 1918 p. 320). Ravn (1918) envisaged
the plant bearing sediments as having been deposited in
a fresh- to brackish-water environment, in which the
rate of deposition equalled the rate of subsidence. The
inoceramids provided evidence of marine conditions and
Ravn therefore concluded that at times subsidence
exceeded deposition and marine environments were
established. Furthermore, he observed no changes in the
style of sedimentation during the Cretaceous and inferred
that deposition had occurred continuously, presumably
within a restricted period and consequently at relatively
high rates of sediment accumulation.
Troelsen (1956) maintained the distinction between
the Kome, Atane and Patoot Formations, quoting descriptions
by Nordenskiöld (1871) and Heer (1883b). These
authors suggested that the Kome and Atane Formations
are separated by a slight angular unconformity (Troelsen
1956).
Koch (1964) regarded the Pautût Formation (sensu
Heer 1883b) as an artificial unit. Henderson et al. (1976
fig. 303) quoted the lithostratigraphy of Troelsen (1956),
but stressed that the Kome, Atane and Pautût formations
lacked formal stratigraphic definition and referred
all the fluvial and deltaic Cretaceous sediments on Disko
and southern to central Nuussuaq to the Atane Formation.
Ehman et al. (1976) used the term Atane Formation
informally for the Cretaceous non-marine deposits and
found that the sediments range in age from Albian through
Santonian.
G.K. Pedersen & Pulvertaft (1992) referred all nonmarine
Cretaceous sediments on Disko and Nuussuaq
to the Atane Formation. They claimed (p. 263) that the
term Atane Formation “had outlived the other formation
names that have been used in the past for the different
isolated outcrops of Cretaceous non-marine strata
in West Greenland”. Based on the data available at that
time, G.K. Pedersen & Pulvertaft (1992 p. 263) interpreted
these strata as “belonging to the same deposi-
55

21’
45’
18’
15’
30’
Uppall
Giesec
Monum
Ivissussat
Qaqqaat
247701
247901
A t a a t a
53°W
247801
Ippigaarsukkløften
1010
K u u a
Paatuut
Paatuutkløften
21’
Ivissussat
Ivisaannguit
Ataa
53°
18’
70°15’N
45’
12’
Fig. 40. Geological map of the south coast of Nuussuaq from Saqqaqdalen to Ivisaannguit, simplified from A.K. Pedersen et al. (2007b). The
type localities of the Atane, Quikavsak and Atanikerluk Formations are all found within this area. The wells GGU 247701, GGU 247801
and GGU 247901 indicated on the map were drilled to obtain technical information on the coal-bearing strata of the Atane Formation.
Contour interval is 200 m; for location, see Fig. 2.
Maligât Formation
Vaigat Formation
Q
Atane Formation
volcanic scree
125 m
Atane
Formation
Fig. 41. Typical outcrop of the Atane Formation at Paatuut on southern Nuussuaq. Note the prominent cyclic alternation of lithologies. For
location, see Fig. 40. Q, Quikavsak Formation; compare with Fig. 14.
56

12’
09’
15’
06’
03’
Saqqaqdalen
Umiusat
Qallorsuaq
Keglen
Naajaat
Kingittoq
Iviangernat
Aasivik
Tartunaq
09’
Vaigat
Nunngarut
52°30’W
06’
Qallunnguaq
Atanikerluk
03’
Aqqullugiaq
Quikassaap Kuua
Qeqertaq
Takisut
5 km
15’
70°N 70°
Quaternary cover
Maligât Formation
Vaigat Formation
Intrusion
Atanikerluk Formation
Quikavsak Formation
Kangilia Formation
Atane Formation
Qilakitsoq Member
Atane Formation
Kingittoq Member
Atane Formation
Undivided
Undifferentiated
pre-Quaternary deposits
Precambrian
Ice
Sea/lake
Borehole
Abandoned settlement
tional system and the same age interval, so that no more
than one formation name seems at present to be required
for the entire non-marine Cretaceous of the area”. Later,
from sedimentological studies, Midtgaard (1996b) argued
for the continued distinction between the Atane, Kome
and Upernivik Næs Formations, as well as for the new
Slibestensfjeldet Formation. Boyd (1993) considered,
mostly on floral evidence, that the sediments at Paatuut
should not be included in the Atane Formation. He
therefore retained the Pautût flora and the Pautût
Formation (Boyd 1993 p. 253). There are, however, no
lithological or sedimentological arguments for retaining
the Pautût Formation of Troelsen (1956) or Boyd (1993),
and we therefore recommend that it be abandoned and
included in the Atane Formation.
Name. From a former settlement Ataa (old spellings
Atane, Atâ) on the south coast of Nuussuaq immediately
west of Ataata Kuua (Figs 2, 3, 40; Nordenskiöld
1871 plate XXI). Today only ruins of a few turf houses
are seen at Ataa.
Distribution. The Atane Formation is restricted to Disko
and Nuussuaq. It comprises the lowermost exposed
deposits on eastern Disko and southern and central
Nuussuaq. Marginally marine successions of Albi an–
Cenomanian age in the northern parts of the Nuussuaq
Basin are referred to the Upernivik Næs Formation.
Exposures of the Atane Formation are found east of
the Disko Gneiss Ridge and east of the Kuugan -
nguaq–Qunnilik Fault (Fig. 10; Chalmers et al. 1999).
On northern Nuussuaq, the Atane Formation is present
east of the Ikorfat fault zone where it overlies the
Slibestensfjeldet Formation (Fig. 22; Midtgaard 1996b).
The distribution of the Atane Formation west of the
outcrop area is little known. There are, however, no sedimentological
data from the Atane Formation to indicate
that the Disko Gneiss Ridge formed a morphological
element during deposition of the formation. Finds of
sandstone xenoliths with chert pebbles in lava flows on
western Disko have been suggested to be derived from
the Atane Formation (Chalmers et al. 1999). The xenoliths
could, however, also have been derived from the
Itilli Formation, which occurs on western Nuussuaq.
Type section. The type section of the formation is the
cored well GGU 247801 (70°19.87´N, 52°55.18´W) in
the gorge of the Ataata Kuua river (Figs 14, 40) where
these sediments were first described by Nordenskiöld
(1871). The next geologist on the site was K.J.V. Steen -
strup. He noted in 1872 that the description given by
Nordenskiöld did not match the outcrop and that the
57

Fig. 42. Well-exposed outcrop at
Paatuut showing the self-combusted
burnt shales (red) that grade into the
typical black-and-white unburnt
sediments of the Atane Formation
(Qilakitsoq Member). Height of
section is approximately 50 m. For
location, see Fig. 40.
burnt shales
geographical position was inaccurate (Steenstrup 1874).
He suggested that Nordenskiöld had measured the type
section of the Atane Formation south-east of the Ataa
river, at “the northern end of the Patoot gorges” (Steen -
strup 1883b p. 64). Later Rosenkrantz (1970 p. 422)
stated that: “... the type locality Atâ, 14 km south-east
of the old village Atâ on the south coast of Nûgssuaq, is
rather close to Pautût..”, but in Henderson et al. (1976)
the type locality of the Atane Formation was again given
at Atâ (Ataata Kuua). The exposures along the western
and eastern slopes of the Ataata Kuua gorge constitute
a long, well-exposed section through the Atane Formation,
and this has been measured photogrammetrically (Fig.
15; A.K. Pedersen et al. 2007b). The sedimentological
log representing the type section (Fig. 43) was measured
in the continuously cored borehole GGU 247801, which
reached a depth of 566 m below terrain (76 m below sea
level).
Reference sections. Skansen, J.P.J. Ravn Kløft, Kingittoq
and Qilakitsoq provide well-exposed reference sections
for the Atane Formation (Figs 48, 51, 53, 60). The two
continuously cored boreholes GGU 247701 and GGU
247901, both from the Paatuut area, are reference boreholes
for the Atane Formation. They comprise strata
from the Qilakitsoq Member and have been described
in detail by Ambirk (2000).
Thickness. The Atane Formation occurs in a number of
fault blocks (J.M. Hansen 1980b; Chalmers et al. 1999;
Marcussen et al. 2001, 2002). The faults are, however,
rarely exposed and although they have been recognised
on seismic profiles acquired in Vaigat and Uummannaq
Fjord (Marcussen et al. 2002), it has not been possible
to determine their throw. Furthermore the lower boundary
of the formation is very rarely exposed. Therefore
the thickness of the Atane Formation can only be given
as an estimate.
The thickest exposed sections occur at Ivissussat on
the south coast of Nuussuaq (700 m) and at Qilakitsoq
on central Nuussuaq (800 m). Seismic data from the
south coast of Nuussuaq show an unconformity at a
depth of 1.5−2 km that has been suggested to represent
the base of the Atane Formation (Christiansen et al.
1995; Chalmers et al. 1999). A seismic line across Vaigat
indicates a minimum thickness of 3000 m for the Atane
Formation (Fig. 44; Marcussen et al. 2001, 2002).
Lithology. The Atane Formation comprises mudstones, heteroliths,
sandstones and coal beds; the relative proportion
of the lithologies varies regionally. The formation is
characterised by aggradation of 10–40 m thick depositional
cycles, which often coarsen upwards (Fig. 45).
The sandstones are typically fine- to medium-grained,
well sorted or heterolithic, with various types of cross-
Facing page:
Fig. 43. Type section of the Atane Formation (and reference section
for the Qilakitsoq Member) from Ataata Kuua, borehole GGU
247801. This core documents the stratigraphic interval known from
the well-exposed section in the Ataata Kuua river gorge and extends
this section down to 76 m below sea level. Tr, transgressive sandstones.
For legend see Plate 1; for location, see Fig. 40.
58

m
0
GGU 247801
200
400
247815 ★
★
50
250
450
Tr
Tr
100
Tr
300
★
500
★
Tr
150
350
Tr
550
★
Tr
vf f m c vc
clay silt sand pebbles
vf f m c vc
clay silt sand pebbles
vf f m c vc
clay silt sand pebbles
59

TWT (msec)
0
500
SP 750
500 250 0
S
Quaternary sediments
N
Fig. 44. Seismic section across the Vaigat
(for location, see Fig. 2; sea level is at
TWT=0). The submarine section continues
into exposures of the formation up to
200–400 m a.s.l. on both sides of Vaigat
indicating a minimum thickness of the
Atane Formation of 3000 m (from
Marcussen et al. 2002). SP, seismic shot
points.
1000
Cretaceous
sediments
c. 0.5 km
1500
1 km
bedding, numerous soft-sediment deformation structures
and local bioturbation. The sandstones consist of
quartz, variably kaolinised feldspars, fragments of older
quartz-rich sedimentary rocks, and small amounts of
mica and other detrital minerals together with comminuted
plant debris. Trace fossils are locally abundant.
The sandstones are cemented by carbonate or clay minerals
but are generally friable. Pervasive cementation is
only patchily developed. The sandstones have sheet or
ribbon geometries.
The mudstones are weakly laminated, typically silty,
with kaolinite as the dominant clay mineral accompanied
by a little mica. The mudstones fall into two groups:
(1) mudstones ranging from silt-streaked mudstone to
df
d
dp
ts
dp
ch
df
ch
Fig. 45. Outcrop of the Atane Formation
in the Paatuut area showing the four
depositional environments characterising
the Atane Formation: delta front (df), delta
plain (dp), fluvial or distributary channel
(ch) and transgressive shoreface deposits
(ts). The delta front deposits form
coarsening-upward units, indicated by
triangular symbols. The dashed lines trace
the bases of delta front mudstones. The
sedimentary succession is cut by a dyke (d).
The thickness of the section is c. 120 m;
for location, see Fig. 40.
60

wave-rippled sand streaked mudstone to heterolithic
sandstone, and (2) mudstones with plant debris, ranging
from carbonaceous mudstone to clayey coal.
The coal beds are interbedded with carbonaceous
mudstones, sand-streaked mudstones and heterolithic
cross-laminated sandstones with local root horizons. The
coal beds are typically less than 0.8 m thick. In several
horizons, coal balls are observed, and silicified wood fragments
are common. The coals belong to the ‘banded
coal’ type dominated by the lithotypes vitrain and clarain.
Macerals of the vitrinite group are often well preserved
owing to the prevailing low rank of the coal. Detailed
study of the organic particles and their geochemistry
permit a distinction between fresh- and brackish-water
environments of coal deposition (Shekhar et al. 1982;
Bojesen-Koefoed et al. 2001; G.K. Pedersen et al. 2006).
The Atane Formation is characterised by depositional
cycles that are typically 10–40 m thick (Figs 41, 46).
The simplest cycles are seen on eastern Disko where they
consist of 10–30 m thick sandstone sheets separated by
c. 5 m thick units of mudstone and coal beds. On southern
and central Nuussuaq, the cycles range in thickness
from 5–15 m up to 40 m. They include coarseningupward
units beginning with mudstones at the base passing
up into heterolithic mudstones, then heterolithic
sandstones with hummocky cross-stratification and ripple
cross-lamination and finally into cross-bedded sandstones,
often with coal debris. The typical coarseningupward
cycle is capped by carbonaceous mudstones with
thin sandstone or coal beds (Pedersen & Pulvertaft 1992
fig. 5). Bioturbated sandstones form part of many cycles.
In the Paatuut area, 32 such cycles have been identified
(Olsen 1991; Dueholm & Olsen 1993).
Fossils. The fossils of the Atane Formation comprise
macroflora, spores and pollen, dinocysts, and invertebrate
fossils (Heer 1868, 1870, 1874a, b, 1880, 1883a,
b; Ravn 1918; Koch 1964; Birkelund 1965; Ehman et
al. 1976; Croxton 1978a, b; Boyd 1990, 1992, 1993,
1994, 1998a, b; Olsen & Pedersen 1991; Koppelhus &
Pedersen 1993; McIntyre 1994a, b, c; Nøhr-Hansen
1996; Lanstorp 1999; Dam et al. 2000).
Macrofossil plants from the Atane Formation are
referred to three floras. The Ravn Kløft flora is characterised
by angiosperms and conifers, and has few species
in common with the Atane flora (Boyd 1998a, b). The
Atane flora is a mixture of older Cretaceous species
together with well-differentiated angiosperm species representative
of many families (Koch 1964; K.R. Pedersen
1976). The Paatuut flora is dominated by conifer and
angiosperm leaf species, and has many species in common
with the Atane flora as well as numerous endemic
species (Koch 1964; Boyd 1992, 1993, 1994).
Spores and pollen occur in most mudstone samples
from the Atane Formation, although often the preservation
is poor or the number of identifiable specimens is low.
Regional studies of the spore and pollen assemblages
have been carried out by Ehman et al. (1976) and Croxton
(1976, 1978a, b). The latter distinguished two stratigraphically
important assemblages, the first without
angiospermous (tricolpate) grains (supposed to be
Cenomanian or older), the second with angiospermous
grains but lacking both Aquilapollenites and complex triporate
grains. The second assemblage was proposed to
be older than Late Campanian (Croxton 1978a p. 76).
A large number of samples from the Cretaceous were
examined on a reconnaissance basis by McIntyre (1994a,
b, c, personal communication 1997) whereas Koppelhus
& Pedersen (1993) and Lanstorp (1999) studied fewer
sections in greater detail.
Marine dinocysts were described from central Nuussuaq
(Ilugissoq, Qilakitsoq, Tunoqqu, southern part of Agat -
dalen) and from southern Nuussuaq (Paatuut, Ataata
Kuua, Nuuk Qiterleq and Nuuk Killeq) by Nøhr-Hansen
(1996), Croxton (1978a, b), McIntyre (1994a, b, c, personal
communication 1997) and Dam et al. (2000).
Brackish-water dinocysts of Late Albian to Cenomanian
age have been described from northern Nuussuaq (Figs
29, 30; Nøhr-Hansen in Sønderholm et al. (2003), Asuk
and in the F93-3-1 core from Kuugannguaq, northern
Disko.
A sparse fauna of marine invertebrates (echinoids and
bivalves) is known from southern and central Nuussuaq
including Sphenoceramus patootensis, Sphenoceramus pinniformis,
and Oxytoma tenuicostata (Ravn 1918; Olsen
& Pedersen 1991). Ammonites from a single horizon at
Alianaatsunnguaq were referred to the Scaphites ventricosus
– Inoceramus involutus Zone by Birkelund (1965);
the Atane Formation in Agatdalen has yielded Baculites
codyensis (Reeside) and radially ribbed inoceramids of
the steenstrupi species-group, an assemblage referred to
the Clioscaphites montanensis Zone (Birkelund 1965;
Dam et al. 2000). Ammonites from the Atane Formation
occur as redeposited fossils in the Itilli Formation on
central Nuussuaq (Dam et al. 2000). Clioscaphites saxitonianus
septentrionalis (Birkelund) has been described
from Ilugissoq, and at Tunoqqo Clioscaphites sp. aff. saxitonianus
(McLearn) occurs together with a single Scaphites
cf. Svartenhukensis (Birkelund 1965; Dam et al. 2000).
Although Koch (1964) suggested that the marine fossils
are restricted to a few horizons, Olsen & Pedersen
(1991) reported that the marine fossils recur through
61

Tr
Tr
Tr
Tr
Tr
Tr
Tr
Tr
Tr
Tr
Tr
Tr
Tr
Tr
50 m
Tr
c. 2 km c. 1 km
Tr
Tr
Fig. 46. Simplified sedimentological logs from the Ivissussat–Paatuut area; colours depict depositional environments, see Plate 1. The logs
document the cyclic depositional pattern and local variations in thickness and lateral changes of facies. Individual phases of delta progradation
may be correlated over short distances between neighbouring sections. The resulting high-resolution lithostratigraphy has only local significance.
For legend, see Plate 1; Tr, Transgressive sand. For location, see Fig. 40.
62

the formation in the marine mudstones at the base of the
delta front cycles. Boyd (1993) also reported marine
invertebrates from several stratigraphic horizons.
Trace fossils are locally abundant and include Dac -
tyoloidites ottoi, Ophiomorpha nodosa, O. irregulaire,
Taenidium serpentinum, Planolites isp., Teichichnus isp.,
Thalassinoides isp., Diplocraterion isp., Skolithos isp.
(Fürsich & Bromley 1985; G.K. Pedersen & Rasmussen
1989; Bojesen-Koefoed et al. 2001; G.K. Pedersen &
Bromley 2006, Bromley & G.K. Pedersen 2008).
Depositional environment. The Atane Formation is interpreted
as having been deposited in a major delta system,
and four depositional environments are distinguished: the
prograding marine delta front, fluvial or distributary
channels of the delta plain, lakes and swamps of the delta
plain, and the marine shoreface.
The coarsening-upward successions of mudstones,
heteroliths and fine-grained sandstones are interpreted
as delta front deposits. In some successions, they include
interdistributary bay deposits (J.M.Hansen 1976; Midt -
gaard & Olsen, 1989; Midtgaard 1991; Olsen 1991;
Olsen & Pedersen 1991; G.K. Pedersen & Pulvertaft
1992; Dueholm & Olsen 1993, Nielsen 2003) (Figs 45,
46). They are interpreted to have resulted from progradation
of shelf deltas sensu Elliott (1989). Olsen (1993)
described channel mouth complexes from the uppermost
part of many delta front cycles at Paatuut.
The fluvial sandstone sheets on eastern Disko are
interpreted as sandy braided river deposits (Johannessen
& Nielsen 1982; Koppelhus & Pedersen 1993; Bruun
2006). These may constitute the multi-storey fill of fluvial
valleys on south-east Nuussuaq (Jensen 2000; Jensen
& Pedersen in press). Fluvial sandstones with ribbon
geometry are interpreted as slightly sinuous distributary
channel deposits (Olsen 1991, 1993). The carbonaceous
mudstones, sandstones and coal seams are interpreted as
freshwater lake or swamp deposits on the delta plain
(Midtgaard 1991; Olsen & Pedersen 1991; G.K. Pedersen
& Pulvertaft 1992; Koppelhus & Pedersen 1993; Nielsen
2003; Møller 2006; G.K. Pedersen et al. 2006). This
facies association is interpreted as representing the vertical
aggradation of a subaerial to shallow limnic, upper
and lower delta plain. The thin beds of sand with marine
trace fossils are interpreted as transgressive sand sheets,
the erosional base of which constitutes a ravinement surface
(Midtgaard 1991; Olsen & Pedersen 1991; G.K.
Pedersen & Rasmussen 1989).
Olsen (1991) and Dueholm & Olsen (1993) documented
32 cycles of delta progradation in the Paatuut
area and comparable numbers of delta cycles are known
from the Qilakitsoq area. J.M. Hansen (1976) observed
that the deltaic cycles in a vertical section at any locality
show a remarkable similarity, indicating an aggradational
stacking pattern. Correlation of individual deltaic
cycles is only possible between closely spaced outcrops
(Fig. 46), but lateral changes in depositional environment
within the Atane Formation may be demonstrated
on a larger scale (Fig. 16).
Boundaries. On Disko, the Atane Formation overlies a
basement high in the FP-93-3-1 well (Fig. 19). On
Nuussuaq, the base of the Atane Formation is exposed
along the north coast where the formation erosively overlies
the Slibestensfjeldet Formation between Ikorfat and
Vesterfjeld (Figs 30, 32). The boundary has been interpreted
either as a minor angular unconformity (Gry 1940;
Koch 1964) or as a conformable, erosional base of a channel
(Ehman et al. 1976; Schiener 1977; Croxton 1978a,
b; Midtgaard 1996b). Midtgaard (1996b) interpreted
the unconformity as a sequence boundary (Fig. 32).
The upper boundary of the Atane Formation is a
marked erosional unconformity (see Fig. 16). On eastern
Disko and Nuussuaq, it is overlain by fluvial and
lacustrine Paleocene deposits of the Atanikerluk For -
mation. On northern Disko, the Atane Formation is erosively
truncated by the Itilli Formation at Kussinerujuk
and Asuk and by the volcanic Vaigat Formation at
Naajannguit (Hald & Pedersen 1975; A.K. Pedersen
1985). Along the south coast of Nuussuaq, the Atane
Formation is unconformably overlain by the marine
Kangilia Formation (Dam et al. 2000), by incised valley
fills of the Quikavsak Formation (Dam et al. 1998a;
Dam & Sønderholm 1998; Dam et al. 2000; Dam 2002),
and by the Eqalulik Formation. In the Aaffarsuaq valley
the Atane Formation is unconformably overlain by the
Itilli Formation (Dam et al. 2000) with rare ammonites
(Birkelund 1965). West of Ilugissoq (central Nuussuaq),
the upper boundary of the Atane Formation is not
exposed.
On northern Nuussuaq, the upper boundary of the
formation can only be seen between Vesterfjeld and
Ikorfat but is generally poorly exposed. Directly east of
the Ikorfat fault zone, the Atane Formation is overlain
by mudstones with Late Campanian to Maastrichtian
ammonites (Birkelund 1965), referred to the Itilli For -
mation. Between Vesterfjeld and Ikorfat, the Atane For -
mation is overlain by the Eqalulik Formation or by
volcanic rocks of the Vaigat Formation (Figs. 22, 29;
A.K. Pedersen et al. 1996, 2006b).
63

Geological age. The scarcity of marine fossils combined
with the long range of many terrestrial plants, spores
and pollen makes it difficult to determine the age of the
Atane Formation with precision; for this purpose not
only the presence but also the abundance of palynomorphs
is important. The age of the formation is bracketed by
the palynomorphs or plant macrofossils in the underlying
Kome and Slibestensfjeldet Formations and by
dinocysts and ammonites in the overlying Itilli Formation
on central and northern Nuussuaq (Fig. 16).
The oldest parts of the Atane Formation are Albi an–
Cenomanian and Early Turonian and occur on Disko,
on southern Nuussuaq at Kingittoq and eastwards, and
on northern Nuussuaq around J.P.J. Ravn Kløft (Croxton
1978a, b; Koppelhus & Pedersen 1993; McIntyre 1994a,
b, c, personal communication 1997; Boyd 1998a, b;
Lanstorp 1999; this study). Sediments of Albian–Ceno -
manian to Turonian age have been reported from Asuk,
and at Kussinerujuk the Atane Formation is overlain by
the Cenomanian Kussinerujuk Member of the Itilli
Formation (McIntyre 1994a, b; Bojesen-Koefoed et al.
2007). The presence of Coniacian deposits is based on
the occurrence of Scaphites ventricosus at Aliana atsun -
nguaq (Birkelund 1965). The youngest parts of the formation
are of Late Santonian to earliest Campanian age
and occur on southern and central Nuussuaq (Paatuut,
Qilakitsoq, Agatdalen; Olsen & Pedersen 1991; Boyd
1992, 1993, 1994; Nøhr-Hansen 1996; D.J. McIntyre,
personal communication 1997; Dam et al. 2000). These
sediments are dated from ammonites (Clioscaphites montanensis
Zone), dinocysts and macroplant fossils (Birke -
lund 1965; Boyd 1992, 1993, 1994; Nøhr-Hansen 1996;
Dam et al. 2000). Coniacian to Early Santonian am mo -
nites in the Itilli Formation on central Nuussuaq overlying
the Atane Formation indicate that the latter is
Santonian or older in this area (Birkelund 1965; Dam
et al. 2000).
Correlation. The Atane Formation is in part coeval with
the marginally marine Upernivik Næs Formation north
of Nuussuaq, and with the lower part of the deep marine
Itilli Formation on Nuussuaq (west of the Kuugan -
nguaq−Qunnilik Fault) and on Svartenhuk Halvø (Figs
13, 16).
Subdivision. The Atane Formation is divided into four
members: the Albian–Cenomanian Skansen Member
and Ravn Kløft Member, the Albian to Lower Turonian
Kingittoq Member, and the Upper Turonian to Santonian
– lowermost Campanian Qilakitsoq Member, which
includes the ?lower Campanian Itivnera Bed.
Skansen Member
new member
History. The Skansen Member includes the sediments
referred to the Atane Formation on southern and eastern
Disko. The coal beds at Skansen were visited by
Giesecke in 1807 and 1811 (in: Steenstrup 1910). He
described the alternation between sandstones and coal
beds, and noted that spherical concretions (Kieskugeln)
are frequent in the sandstones. The history of coal mining
at Skansen was summarised by K.J.V. Steenstrup,
who also measured a geological profile of the coastal cliff
at Skansen (Steenstrup 1874 plate VIII).
Name. The name is taken from the former settlement
Skansen (old spelling Skandsen) or Aamaruutissat, on the
south coast of Disko (Fig. 124). The name ‘Skansen’
(meaning rampart or palisade) originates from a thick and
very prominent sill of columnar jointed basalt, named
Innaarsuit in Greenlandic.
Distribution. The Skansen Member crops out on southern
and eastern Disko (Figs 124, 132; A.K. Pedersen et
al. 2000, 2001, 2003). The sediments are exposed in
stream sections along the coast and in the inland valleys
such as Kvandalen and Laksedalen. The Skansen Member
is not known from wells and its distribution outside the
area of outcrop is unknown. The Cretaceous sediments
recorded in seismic sections in Disko Bugt south and
east of Disko (Chalmers et al. 1999) presumably in part
belong to the Skansen Member.
Type section. The type section of the Skansen Member is
on the south-facing slope behind the settlement of Skansen
(Figs 47, 48, 124). The sedimentology and palynology
of this section have been studied in some detail (Koppelhus
& Pedersen 1993; Bruun 2006; Møller 2006a, b). The
base of the type section is located at 69°26.40´N,
52°26.32´W.
Reference sections. Reference sections are found at
Illunnguaq (Koppelhus & Pedersen 1993) and Pingu
(Fig. 132).
Thickness. Only the upper 470 m of the Skansen Member
are exposed. However, geophysical data indicate that sediments
with a thickness of c. 2 km are present east of Disko
(Chalmers et al. 1999), suggesting that the Skansen
Member may reach a considerable thickness in the subsurface.
64

d
d
Fig. 47. Type locality of the Skansen Member of the Atane Formation at Skansen, southern Disko (for location, see Fig. 124). The Skansen
Member is dominated by fluvial sandstones, interbedded with fine-grained floodplain deposits and thin coal seams. The peak is at 470 m
a.s.l. and the sediments are cut by several dykes (d).
Lithology. The Skansen Member is dominated by white
to yellow sandstones with sheet geometry, intercalated
with coal seams, mudstones and heteroliths rich in plant
debris arranged in a cyclic depositional pattern (Figs 47,
49). Sixteen cycles are recognised, typically 20–30 m
thick (Bruun 2006). The sandstones consist of quartz,
more or less kaolinised feldspars, fragments of older
quartz-rich sedimentary rocks, and small amounts of
mica and other detrital minerals together with comminuted
plant debris. The sandstones are generally friable,
since carbonate or clay mineral cement is only
locally developed. The sandstones are medium- to coarsegrained,
in places with pebbly channel lags of intraformational
mudstones, coal clasts or pebbles of chert and
Ordovician limestone (A.K. Pedersen & Peel 1985). They
are dominantly cross bedded or structureless (Fig. 49),
but commonly show soft-sediment deformation structures.
Sandstone sheets with a width: thickness ratio in
excess of 15 are characteristic. The interbedded finegrained
sediments are dark grey to black due to the ubiquitous
presence of comminuted plant debris. Facies vary
rapidly both vertically and laterally between heterolithic,
cross laminated sand, mudstone with plant debris, massive
brownish mudstone and coal beds, most of which
are less than 1 m thick. Locally, root horizons or rare tree
stumps are present. The coal beds are c. 0.5 m thick, and
the coals are subbituminous, with up to 20% siliciclastic
particles and very little pyrite. The coals are dominated
by huminite which originates from wood and plant tissue
rich in cellulose (Møller 2006a, b).
Fossils. Macroflora, spores and pollen are known from the
Skansen Member (Heer 1883a, b; Seward 1926; Miner
1932a, b, 1935; Ehman et al. 1976; Croxton 1978a, b;
Koppelhus & Pedersen 1993). The plant fossils from six
localities (Innanguit, Killusat, Skansen, Pingu, Ujara -
sussuk, Illukunnguaq) were referred to the Atane flora
by Heer (1883b p. 93). Assemblages of palynomorphs
65

m
130
m
Fig. 48. Type section of the Skansen
Member; note the dominance of fluvial
channel deposits, (see also Figs 47 and 49).
Base of section is at c. 120 m a.s.l. For
legend, see Plate 1.
110
50
250
0
200
mud
sand
180
mud
sand
have been studied at reconnaissance level at Marraat
(southern Disko) and Skansen (Ehman et al. 1976), at
Kuuk Quamasoq and Pingu (Croxton 1978a, b; D.J.
McIntyre, personal communication 2003) and in more
detail at Skansen and Illunnguaq (Koppelhus & Pedersen
1993) (Fig. 124).
Depositional environment. The sandstone sheets in the
Skansen Member are interpreted as sandy braided river
deposits. The sediment transport directions on eastern
Disko vary from north-north-west at Pingu to southwest
at Gule Ryg and Skansen (G.K. Pedersen & Pulvertaft
1992 fig. 6), suggesting the presence of a huge alluvial
cone with its apex east of Disko. Apparently, the Disko
Gneiss Ridge did not affect the depositional pattern of
the Skansen Member (Johannessen & Nielsen 1982;
G.K. Pedersen & Jeppesen 1988; Koppelhus & Pedersen
1993; Bruun 2006).
The carbonaceous mudstones, sandstones and coal
seams are interpreted as freshwater lake or swamp deposits
representing the vertical aggradation of a subaerial to
shallow, limnic floodplain to upper delta plain. The
66

Fig. 49. Cross-bedded medium- to coarsegrained
fluvial sandstones of the Skansen
Member at Skansen. Note the intraformational
conglomerate (C) composed of
mudstone and coal clasts (lower part of
photo), and the thin interval of carbonaceous
mudstone (floodplain deposits; fp)
in the upper part.
fp
c. 20 m
C
spores and pollen represent vegetation dominated by
conifers and ferns; there are no indications – neither
palynological evidence nor the presence of pyrite – to suggest
marine or brackish-water conditions (G.K. Pedersen
& Pulvertaft 1992; Koppelhus & Pedersen 1993; Møller
2006).
Boundaries. The lower boundary of the Skansen Member
is not exposed. The upper boundary is an erosional
unconformity overlain by the Paleocene Atanikerluk
Formation. At Pingu, the Skansen Member is overlain
by fluvial sand of the Akunneq Member (Figs 16, 132),
while it is overlain by lacustrine mudstones of the Assoq
Member at Tuapaat on southern Disko. The presence of
late Cenomanian or Turonian strata at the top of the
Illunnguaq section was suggested by Koppelhus &
Pedersen (1993), but was not confirmed by examination
of additional samples. The upper boundary of the
Skansen Member corresponds to the upper boundary of
the Atane Formation in the area where the Skansen
Member occurs.
Geological age. The Skansen Member is dated on the
basis of spores and pollen. At its type locality, a mid-
Cenomanian age seems most likely, with a maximum
age range of Late Albian to Cenomanian for the palynomorph
assemblages from this member (Croxton 1978a,
b; Ehman et al. 1976; Koppelhus & Pedersen 1993).
Correlation. The fluvial Skansen Member is laterally
equivalent to the deltaic Kingittoq Member on northern
Disko (between Qullissat and Kussinerujuk), and
on southern Nuussuaq (between Atanikerluk and
Kingittoq) (Fig. 16). The Skansen Member also correlates
with the fluviodeltaic Ravn Kløft Member on northeastern
Nuussuaq and in part at least with the Upernivik
Næs Formation on Upernivik Ø. Palynomorphs are not
preserved in the lower part of the Itilli Formation on
Svartenhuk Halvø and on western Nuussuaq, which precludes
firm correlation between the Skansen Member
and the Itilli Formation (Figs 13, 16).
Ravn Kløft Member
new member
History. The Ravn Kløft Member is part of the Cretaceous
succession overlying the Slibestensfjeldet Formation on
north-eastern Nuussuaq. These sediments have previously
been referred to the Atane Formation (Nordenskiöld
1871; Gry 1942; Midtgaard 1996b) or to the Upernivik
Næs Formation (Rosenkrantz 1970; Henderson et al.
1976).
Name. The member is named after the gorge J.P.J. Ravn
Kløft where it forms impressive outcrops (Fig. 50A, B).
J.P.J. Ravn studied the geology of the Nuussuaq Basin
in 1909, with focus on the marine invertebrates from the
region (Ravn 1918).
Distribution. The Ravn Kløft Member is known from outcrops
along the north coast of Nuussuaq between Ikorfat
67

A
Kingittoq
Member
Ravn Kløft
Member
c. 60 m
B
Fig. 50. A: Type locality of the Ravn Kløft Member on the west-facing slopes of the J.P.J. Ravn Kløft gorge on Slibestensfjeldet. Note the very
thick fluvial sandstone bodies at the top of the Ravn Kløft Member that can be traced westwards to Ikorfat. The Ravn Kløft Member is overlain
by the Kingittoq Member (Atane Formation). For location, see Fig. 22. B: Large-scale cross-bedding in sandstones of the thick, amalgamated
fluvial channel deposits at the top of the Ravn Kløft Member at Ravn Kløft (c. 395 m in Fig. 51A). The height of the exposure is c. 3 m.
68

and Qaarsut (Fig. 22). Its wider distribution is not known
due to lack of exposures.
Type section. The eastern slope of J.P.J. Ravn Kløft constitutes
the type section (Figs 22, 51A). The base of the
type section is located at 70°45.18´N, 52°55.08´W.
Reference sections. Reference sections are found in stream
exposures just east of Ikorfat, at Slibestensfjeldet and at
Vesterfjeld (Figs 22, 51B, 52).
Thickness. The thickness of the Ravn Kløft Member is
about 450 m in the type section, thinning both towards
the east and the west (Midtgaard 1996b). The basal pebbly
sandstone varies in thickness from less than 2 m to
a maximum of 56 m. The overlying deposits are c. 400
m thick in J.P.J. Ravn Kløft.
Lithology. A variety of lithologies and sedimentary facies
are present in the Ravn Kløft Member. The member is
tripartite, comprising a lower pebbly sandstone unit, a
middle unit of mudstones, heteroliths and fine-grained
sandstones with coarsening-upward or fining-upward
depositional patterns, and an upper unit of thick-bedded
medium- to coarse-grained sandstones interbedded
with mudstones and heteroliths (Fig. 50B; Midtgaard
1996b). The lower unit (c. 35–62 m on Fig. 51A) includes
a c. 3 m thick conglomeratic sandstone with rounded pebbles
and large clasts of coaly mudstone, fossil wood and
mudstone, interpreted as a channel lag. This is overlain
by pebbly coarse-grained sandstones with large-scale
cross-bedding, followed by coal-bearing mudstones with
beds consisting of small Scaidopityoides leaves (Midtgaard
1996b). The cross-bedding indicates unidirectional northward
sediment transport.
The middle unit (c. 62–340 m on Fig. 51A) comprises
a variety of facies. Coarsening-upward successions
comprise laminated mudstones, heterolithic sandstones
and hummocky cross-stratified sandstones, which locally
are capped by trough cross-bedded sandstones, mudstones
with root horizons and thin coal beds. Wave-ripple
crests are oriented ESE–WNW. Comminuted car -
bonaceous debris is abundant. Fining-upward successions
comprise medium- to coarse-grained, well-sorted
sandstones with cross-bedding, double mud-drapes, and
abundant reactivation surfaces. They are overlain by heteroliths
with current and wave ripple cross-lamination
followed by black, laminated mudstones. Synaeresis
cracks are common.
The upper unit (c. 340–400 m on Fig. 51A) of the
Ravn Kløft Member consists of thick, erosively based
bodies of greyish sandstone alternating with dark heterolithic
mudstone. The sandstones are fine- to coarsegrained
or conglomeratic, and dominantly cross-bedded.
Foresets are often oversteepened and large-scale soft-sediment
deformation structures are very common (Fig.
52). Composite sandstone bodies may be up to 60 m thick
(Fig. 50), and may extend laterally for at least 8 km. The
cross-bedding indicates sediment transport to the
NE–N–NW. The sandstone bodies alternate with thinly
interbedded rippled sandstones, laminated mudstones
and heteroliths containing abundant rootlets and plant
fossils, thin coal beds and palaeosols at certain levels.
Fossils. A brackish-water dinocyst assemblage dominated
by Nyktericysta davisii has been identified in a number
of the mudstone beds. The pollen Rugubivesiculites rugosus
has its first stratigraphical occurrence within the member
(Fig. 29).
Depositional environment. The lower unit of the Ravn
Kløft Member is interpreted as a basal fluvial valley-fill
conglomerate overlain by fluvial sandstones deposited
by unidirectional northward-flowing currents. The middle
units are interpreted as interbedded deltaic and tidal
estuarine deposits, and wave-ripple crestlines suggest an
ESE–WNW-oriented coastline. The overlying single to
multi-storey sandstone bodies represent a variety of fluvial
styles from slightly sinuous single channels to braided
rivers with multiple channels and northward palaeocurrents.
The presence of rootlets, vitrinite lenses and local
coal beds in the floodplain sandstones and mudstones
indicates the existence of a range of sub-environments
from subaerial floodplain to shallow-water swamps or
ponds adjacent to the fluvial channels. The fluvial sandstones
show an increasing tendency up-section to amalgamate
and form thick, multi-storey sandstone sheets
(Midtgaard 1996b).
Boundaries. The lower boundary of the Ravn Kløft
Member is the same as for the Atane Formation. The
thickness variation of the lower fluvial sandstones of the
Ravn Kløft Member suggests that the base had a relief
of nearly 55 m on a regional scale (Midtgaard 1996b).
The upper boundary is placed at the top of a c. 60 m
thick, amalgamated multi-storey fluvial sandstone sheet
which is abruptly overlain by a succession of interbedded
mudstones, heteroliths, sandstones and thin coal
seams referred to the Kingittoq Member (Fig. 50).
Geological age. Based on the palynomorphs, the Ravn
Kløft Member is assigned a Late Albian – Early Ceno -
69

A
m
B
m
150
300
Atane Formation
Ravn Kløft Member
100
50
Ravn Kløft Member
250
200
Ravn Kløft Member Kingittoq Member
450
400
100
Atane Formation
Ravn Kløft Member
50
Kingittoq Member
Ravn Kløft Member
250
200
Slibestensfjeldet Formation
0
350
mud sand mud sand mud sand mud sand mud sand
Slibestensfjeldet Fm
150
0
Fig. 51. A: Type section of the Ravn Kløft Member at J.P.J. Ravn Kløft. B: Reference section at Ikorfat. The thick sandstone beds at the top
of the member are overlain by the Kingittoq Member. For legend, see Plate 1; for location, see Fig. 22.
70

Fig. 52. Two closely spaced sections
through the Ravn Kløft Member showing
the rapid lateral facies changes especially of
the fluvial channel deposits. The sections
correspond approximately to the interval
255–285 m in Fig. 51A. For legend, see
Plate 1; for location, see Fig. 22.
SE
m
30
Tidal–estuarine
m
30
NW
20
20
Lacustrine
10
10
Fluvial
valley
fill
0
mud
sand
gravel
base 495 m a.sl.
0
mud sand gravel
40 m
manian age (Ehman et al. 1976; Croxton 1978a, b; this
study). A distinct macroflora (the Ravn Kløft flora) of
Middle Albian to Early Cenomanian age was established
by Boyd (1998a, b, c, 2000); this flora was broadly contemporaneous
with the Upernivik Næs flora of Rosen -
krantz (1970).
Correlation. The Ravn Kløft Member is laterally equivalent
to the Skansen Member in southern and eastern
Disko and the older parts of the Kingittoq Member on
central and southern Nuussuaq and northern Disko. The
Ravn Kløft Member is possibly coeval with the lower
part of the Itilli Formation on western Nuussuaq and
Svartenhuk Halvø and with parts of the Upernivik Næs
Formation on Upernivik Ø (Fig. 16).
Kingittoq Member
new member
History. The Kingittoq Member includes the sediments
referred to the Atane Formation on northern Disko,
south-eastern Nuussuaq, as well as some of those on
northern Nuussuaq.
71

160
150
140
130
120
110
100
90
80
70
60
50
40
30
20
10
330
320
310
300
290
280
270
260
250
240
230
220
210
200
190
180
170
m
490
480
470
460
450
440
430
420
410
400
390
380
370
360
350
340
0
vf f m c vc f m c
clay silt sand pebbles
vf f m c vc f m c
clay silt sand pebbles
vf f m c vc f m c
clay silt sand pebbles
Fig. 53. Type section of the Kingittoq Member of the Atane Formation at Kingittoq, south coast of Nuussuaq (for location, see Fig. 40). Note
the higher proportion of delta channel deposits compared to the Qilakitsoq Member (Fig. 60). Compare with Figs 54 and 55 to appreciate
the facies variations within the member. Marine dinocysts are only found in a few of the delta front units. For legend, see Plate 1.
Name. The member is named from the coastal slopes at
Kingittoq on the south coast of Nuussuaq, where it is
well exposed (Fig. 40).
Distribution. The Kingittoq Member is known from outcrops
on southern Nuussuaq from Saqqaqdalen to
Kingittoq, on northern Disko from Qullissat to
Kussinerujuk, and on northern Nuussuaq from Vesterfjeld
to Ikorfat (Figs 2, 22, 40, 50A).
72

Type section. The type section of the Kingittoq Member
is exposed in the slopes at Kingittoq on southern Nuussuaq
(Figs 40, 53, 59). The base of the type section is located
at 70°09.77´N, 52°31.38´W.
m
Reference sections. Reference sections are found in the
upper reaches of J.P.J. Ravn Kløft and at Asuk (Figs 54,
55).
Thickness. The thickness of the Kingittoq Member is not
known, but it probably exceeds 1 km. In the area of the
type section, more than 600 m are exposed (A.K. Pedersen
et al. 2007a), c. 450 m are exposed at Kuussinerujuk and
up to 150 m are exposed above the Ravn Kløft Member
on northern Nuussuaq.
Lithology. On southern Nuussuaq, the Kingittoq Member
is characterised by 10−25 m thick depositional cycles,
which comprise coarsening-upward successions of mudstones,
heteroliths and well-sorted sandstones (Figs
53–58). Complex sandstone sheets, up to 40 m thick,
are often overlain by carbonaceous heterolithic mudstones
with thin coal beds and constitute fining-upward
successions (Figs 53, 59). In the Atanikerluk area, the complex
sandstone sheets constitute c. 40% of the section
(Nielsen 2003) whereas their proportion is higher in
Saqqaqdalen (Shekhar et al. 1982) and at Kussinerujuk
(Pulvertaft & Chalmers 1990). The member is characterised
by aggradational stacking of the depositional
cycles (Figs 57, 58).
The sandstones are pale, friable, medium- to coarsegrained,
in places with pebbly channel lags of intraformational
mudstone or coal clasts, and are either crossbedded
or structureless, commonly with soft-sediment
deformation structures (Midtgaard 1991; Olsen 1991;
G.K. Pedersen & Pulvertaft 1992; Jensen 2000; Nielsen
2003; G.K. Pedersen et al. 2006). The mudstones are grey,
silty, carbonaceous, at several localities with high C/S
ratios, and are weakly laminated (Nielsen 2003). The
mineralogy is similar to that in the rest of the Atane
Formation. The coal beds are interbedded with mudstones
with plant debris, sand streaked mudstones and
cross laminated sand. Root horizons are seen locally, but
preserved tree stumps are rare. A few of the coal beds have
been studied in detail (Shekhar et al. 1982; Bojesen-
Koefoed et al. 2001; G.K. Pedersen et al. 2006). Coars -
ening-upward successions of grey mudstones, wave-rippled
heterolithic sandstones and fine-grained sandstones with
swaley and hummocky cross stratification are especially
well developed at Asuk (Fig. 56). The sedimentary structures
are enhanced by drapes of comminuted plant (coal)
40
30
20
10
0
mud sand gravel
Fig. 54. Reference section of the Kingitoq Member at J.P.J. Ravn Kløft
(for location, see Fig. 22). Note the predominance of delta plain
facies deposited in shallow lakes, small channels and interdistributary
bays. See also Fig. 51A. Base of section at c. 650 m a.s.l. For legend,
see Plate 1.
73

m
m
140
130
Itilli Formation
Kussinerujuk Member
20
10
0
120
Tr
vf f m c vc
clay silt sand
110
Atane Formation
Kingittoq Member
100
90
80
70
Tr
Fig. 55. Reference section of the Kingittoq
Member at Asuk, north coast of Disko (for
location, see Fig. 2). The section is domi -
nated by stacked delta front deposits and
intervals assigned to the delta plain facies
association are thin. Note that only one
thin coal seam is present (44 m). See also
Figs 56, 57 and 80. At this locality, the
member is clearly more influenced by
marine deposition than at Kingittoq (Fig.
53). Tr, transgressive sandstones. For
legend, see Plate 1.
60
Tr
Tr
50
40
30
20
10
0
vf f m c vc
clay silt sand
Tr
Tr
Tr
debris. Marine fossils are found locally and bioturbation
is generally slight. Thin beds of well-sorted, structureless
sandstone are seen at Kingittoq, whereas similar
beds at Asuk show erosional bases and contain numerous
trace fossils, of which Ophiomorpha nodosa is prominent
(Fig. 55).
Fossils. Plant macrofossils, spores and pollen are known
from the Kingittoq Member (Heer 1883a, b; Seward
1926; Ehman et al. 1976; Croxton 1978a, b; Lanstorp
1999). Heer (1883b) described plant fossils collected
from four outcrops of the Kingittoq Member (Qullissat,
Asuk, Qallunnguaq, and Atanikerluk) and referred these
to the Atane flora and the Patoot flora.
Marine dinocysts are known from the Kingittoq
Member (D.J. McIntyre, personal communication 1997)
and finds of rare individuals of three marine invertebrates,
Nucula cancellata, Nucula sp., and Lucina occidentalis,
were reported from Kingittoq (Ravn 1918). The
trace fossils Ophiomorpha nodosa, Taenidium serpentinum,
Teichichnus rectus, Thalassinoides isp. occur locally in the
Kingittoq Member.
74

Fig. 56. Delta front succession of the
Kingittoq Member at Asuk (27–35 m in
Fig. 55). Note the upward increase in
frequency and thickness of sandstone beds.
The well-sorted sandstones with hummocky
and swaley cross-stratification (S)
are indicative of a high-energy depositional
environment. The mudstone (M) at the
top of the section is interpreted as an
interdistributary bay deposit. For location,
see Fig. 2.
M
S
delta front
Depositional environment. The Kingittoq Member is interpreted
to represent fluvial to deltaic deposits and is
referred to four facies associations: the channel and delta
plain associations (dominant), the delta front or mouth
bar association (subordinate) and the transgressive sand
sheet association (rare) (Midtgaard 1991; G.K. Pedersen
& Pulvertaft 1992; Dam et al. 2000; Jensen 2000; Nielsen
2003; G.K. Pedersen et al. 2006). The cross-bedded,
medium- to coarse-grained sandstones are interpreted
as fluvial channel deposits. The sedimentary structures
frequently indicate downstream accretion on bars and rare
development of point bars, indicating that the fluvial
channels were mostly braided. The complex sheets of
coarse-grained sandstones are interpreted as having been
deposited as the multi-storey fill of fluvial valleys (Jensen
2000; Jensen & Pedersen in press).
The carbonaceous mudstones, sandstones and coal
beds are interpreted to represent the vertical aggradation
of subaerial to freshwater lacustrine or swamp deposits.
The high C/S ratios indicate that deposition occurred in
freshwater environments on the upper delta plain (G.K.
Pedersen & Pulvertaft 1992; Nielsen 2003). The coal
beds are interpreted as the in situ accumulations of plant
remains in freshwater environments (Bojesen-Koefoed et
al. 2001; G.K. Pedersen et al. 2006). This facies association
is subordinate at Asuk.
The coarsening-upward heteroliths are interpreted as
delta front or mouth bar deposits formed during progradation
of shelf deltas (G.K. Pedersen & Pulvertaft 1992;
Bojesen-Koefoed et al. 2001; Nielsen 2003; G.K. Pedersen
et al. 2006). This facies association is dominant at Asuk.
The thin beds of sand with marine trace fossils are interpreted
as transgressive sand sheets (Midtgaard 1991).
The erosive base constitutes a ravinement surface. In the
Kingittoq Member, the transgressive sand sheets are best
developed at Asuk. The Kingittoq Member is dominated
by stacked upper delta plain deposits in the Atanikerluk
area and at Qullissat, and by lower delta plain and stacked
delta front deposits at Asuk.
Boundaries. The lower boundary of the Kingittoq Member
is exposed on northern Nuussuaq where the Kingittoq
Member overlies the Ravn Kløft Member (Fig. 50). Here
the boundary is a drowning surface which separates the
fluvial sandstones from the overlying delta plain deposits.
In the rest of the Nuussuaq Basin, the lower boundary
is not exposed.
The upper boundary, corresponding generally to the
upper boundary of the Atane Formation in the outcrop
area of the member, is everywhere an erosional unconformity
overlain by the Itilli, Quikavsak, Atanikerluk
and Vaigat Formations (Fig. 16). On the north coast of
75

delta front
ts
channel
channel
25 m
delta front
ts
delta front
delta front
ts
ts
Fig. 57. The Kingittoq Member at Asuk showing thick fluvial channel deposits overlying coarsening-upward delta front successions capped
by transgressive shoreface sandstones (ts). For location, see Fig. 2 and Fig. 55: 44–83 m.
Nuussuaq, the upper boundary of the Kingittoq Member
is generally poorly exposed due to landslides and rock
glaciers, but east of Ikorfat it is overlain by small outcrops
of Campanian–Maastrichtian mudstone (the Itilli For -
mation) and Paleocene tuffaceous mudstone (the Eqalulik
Formation) (Birkelund 1965; A.K. Pedersen et al. 2006b)
(Fig. 22).
channel
delta plain
delta front
channel
delta plain
delta front
delta plain
channel
delta front
delta plain
channel
30 m
Fig 58. Outcrop of the Kingittoq Member
on the eastern slope of the Qallunnguaq
valley (for location, see Fig. 40). Delta
plain facies constitute a large proportion
of the succession and delta front deposits
are thin and fine-grained suggesting lowenergy
depositional environments (lower
delta plain with swamps, shallow lakes and
interdistributary bays (Nielsen 2003)). The
channel sandstone at the top of the photo -
graph is the lowermost fluvial unit in a
multi-storey sandstone body studied by
Jensen (2000) and Jensen & Pedersen (in
press).
76

Fig. 59. The Kingittoq Member at King -
ittoq, see 310–465 m in Fig. 53. Most
fluvial channels are braided, but a point
bar succession is seen in the centre of the
photo with inclined accretionary surfaces
(indicated by dotted line); ch, fluvial
channel; df, delta front. For location, see
Fig 40.
Atanikerluk Formation
sill
Atane Formation
df
ch
ch
Geological age. The geological age of the Kingittoq Member
ranges from Albian (Tartunaq) to Cenomanian (Atani -
kerluk, Saqqaqdalen, Kingittoq, Kussinerujuk, Asuk and
Ravn Kløft) and into Early Turonian (Saqqaqdalen,
Kingittoq and Asuk). The deposits are dated on the basis
of spores, pollen and marine dinocysts (Croxton 1978a,
b; Lanstorp 1999; McIntyre 1994a, personal communication
1997; this study).
Correlation. The Kingittoq Member is coeval with the
Skansen Member (eastern Disko); the Kingittoq Member
of southern Nuussuaq may be equivalent the Ravn Kløft
Member on northern Nuussuaq (Fig. 16). The Kingittoq
Member correlates with the Upernivik Næs Formation
on Upernivik Ø, and possibly to the lower part of the
Itilli Formation of western Nuussuaq and Svartenhuk
Halvø.
Qilakitsoq Member
new member
History. The Qilakitsoq Member includes sediments
referred to the Atane Formation on southern and central
Nuussuaq, and sediments formerly referred to the now
abandoned Pautût (or Patoot) Formation (see above
under history of the Atane Formation).
Name. The name is derived from the Qilakitsoq stream,
a tributary to the Kuussuaq river which flows through
the Aaffarsuaq valley on central Nuussuaq (Fig. 82).
Distribution. The Qilakitsoq Member is the sole representative
of the Atane Formation in central Nuussuaq and
parts of southern Nuussuaq. Outcrops are found from
Agatdalen to Ilugissoq along the north slope of the
Aaffarsuaq Valley and along the south coast from Paatuut
to Alianaatsunnguaq (Figs 2, 40, 82).
Type section. The type section of the Qilakitsoq Member
is along the Qilakitsoq stream on central Nuussuaq (Figs
60, 82). The base of the type section is located at
70°27.97´N, 53°27.13´W.
Reference sections. Reference sections are found at Nuuk
Killeq and Ataata Kuua (type section of the Atane
Formation; Fig. 43). Two continuously cored boreholes
from the Paatuut area (GGU 247701 and GGU 247901)
provide reference sections of the Qilakitsoq Member and
have been described in detail by Ambirk (2000).
Thickness. The type section documents a minimum thickness
of 480 m, but correlation with nearby sections shows
that at least 820 m are exposed in the Qilakitsoq area,
and c. 600 m are known from the well at Ataata Kuua
together with nearby outcrops (Fig. 43; A.K. Pedersen
et al. 2007b).
Lithology. The Qilakitsoq Member is characteristically
cyclic, individual cycles typically passing up from mudstones
through heteroliths, well-sorted sandstones, coarser
grained sandstones with ribbon geometry, and finally
into carbonaceous mudstones with coal beds overlain by
thin sheets of bioturbated sandstone (Fig. 60; Midtgaard
77

m
480
160
470
150
310
460
140
300
450
130
290
440
120
280
430
110
270
420
100
260
410
90
250
400
80
240
390
70
230
380
60
220
370
50
210
360
40
200
350
30
190
340
20
180
330
10
170
320
0
vf f m c vc f m c
clay silt sand pebbles
vf f m c vc f m c
clay silt sand pebbles
vf f m c vc f m c
clay silt sand pebbles
Fig. 60. Type section of the Qilakitsoq Member (Atane Formation) on the western side of the Qilakitsoq stream, central Nuussuaq. Note the
higher proportion of delta front deposits compared to the Kingittoq Member (Fig. 53). For location, see Fig. 82; for legend, see Plate 1.
1991; Olsen 1991, 1993; G.K. Pedersen & Pulvertaft
1992; Boyd 1993; Dueholm & Olsen 1993; Ambirk
2000; Dam et al. 2000). The coarsening-upward successions
are typically 5−25 m thick but may reach up to
c. 70 m (Fig. 61). They can be traced laterally through
closely spaced outcrops for up to 8 km in the Paatuut
area (Fig. 46; Olsen 1991, 1993; Dueholm & Olsen1993)
and also in the Qilakitsoq area.
The mudstones at the base of the coarsening-upward
units are dark grey, silty and weakly laminated, and may
contain marine fossils (Olsen & Pedersen 1991; Nøhr-
Hansen 1996). These grade up into sand streaked mudstones
and heterolithic sandstones, where wave-ripples
and swaley- and hummocky cross-stratification are
enhanced by drapes of comminuted plant debris (Fig. 60,
33–50 m). The successions are frequently topped by
medium-grained, trough cross-bedded sandstones (Fig.
60, 145-158 m). Bioturbation may locally be very intense
and totally obscure primary structures.
78

sh
L
sh
ch
delta front
Vaigat Formation
Atane
Formation
65 m
Fig. 61. Outcrop of the Qilakitsoq Member on the western slope of
gully immediately west of Qilakitsoq. The member is dominated by
stacked delta front successions. The outcrop corresponds to the interval
200–380 m in Fig. 60; ch, channel; L, lagoon; sh, shoreface.
Note that the uppermost delta front succession is abnormally thick
at this locality. For location, see Fig. 82.
Other sandstones are pale, friable, medium- to coarsegrained,
in places with channel lags of pebbles or intraformational
clasts of mudstone and coal. These sandstones
are cross bedded or structureless, commonly with softsediment
deformation structures. They form single-storey
sandstone ribbons with a width:thickness ratio as low as
6 and a sinuosity of 1.2 (Olsen 1993) (Fig. 60: 0–11 m).
Successions of carbonaceous heteroliths interbedded
with cross laminated sand, sand streaked mudstones,
mudstones with plant debris and coal seams occur in all
outcrops of the Qilakitsoq Member. Their dark grey to
black colour reflects the abundance of comminuted plant
debris. Locally, root horizons or rare tree stumps are present.
Numerous coal beds at Paatuut and Ataa are more
than 0.8 m thick. Concretions and ‘coal balls’ are observed
in several horizons, as well as silicified wood. Dirt bands
in coal beds are common, mainly consisting of carbonaceous
mudstones (Fig. 60: 20–32 m).
Sheets of structureless or strongly bioturbated sandstone
with an erosional base occur in most outcrops of
the Qilakitsoq Member. They range from thin (c. 0.05
m) fine-grained sandstones to thick (c. 3 m) mediumto
coarse-grained sandstones. Upwards, these sandstones
may pass gradually into mudstones (Fig. 60, 180–182 m).
Fossils. Plant macrofossils, spores and pollen are known
from the Qilakitsoq Member (Heer 1883a, b; Seward
1926; Ehman et al. 1976; Croxton 1978a, b; Boyd 1990,
1992, 1993, 1994). Heer (1883b) described plant fossils
collected from three outcrops of the Qilakitsoq
Member (Alianaatsunnguaq, Ataa, and Paatuut) and
referred these to the Atane and Patoot floras. Boyd (1992,
1993) recognised three or more floral communities
(nearshore lacustrine, backswamp, levee and riparian
vegetation) in the fossil flora from the Paatuut area (the
Paatuut flora).
Marine dinocysts have been identified in samples from
the Qilakitsoq Member (D.J. McIntyre, personal communications
1997, 1999; Nøhr-Hansen 1996). The
sparse marine invertebrates include ammonites (Clioscaphites
saxitonianus septentrionalis (Birkelund), Clioscaphites
sp. aff. saxitonianus (McLearn), Scaphites ventricosus,
Scaphites cf. Svartenhukensis, and Baculites codyensis
(Reeside)) (Birkelund 1965; Dam et al. 2000); bivalves
(Sphenoceramus patootensis, S. pinniformis, Oxytoma
tenuicostata) and echinoderms (Ravn 1918; Olsen &
Pedersen 1991; Boyd 1993).
Trace fossils are common in the Qilakitsoq and Nuuk
Killeq areas. Burrows such as Planolites isp., Teichichnus
isp., Dactyolidites ottoi, and Helminthopsis horizontalis
occur in the coarsening-upward successions, whereas
Ophiomorpha nodosa and O. irregulaire are seen in the
sandstone sheets (Fig. 62; G.K. Pedersen & Rasmussen
1989; Dam et al. 2000; G.K. Pedersen & Bromley 2006).
The trace fossil assemblages indicate the presence of both
suspension and deposit feeders.
Depositional environment. The Qilakitsoq Member is
interpreted as being constructed of aggradational deltaic
deposits referred to four facies associations: the marine
delta front association, the distributary channel association,
the delta plain association and the transgressive sand
sheet association (Midtgaard 1991; Olsen 1991, 1993;
G.K. Pedersen & Pulvertaft 1992; Dueholm & Olsen
1993; Dam et al. 2000).
79

Fig. 62. The trace fossil Ophiomorpha
irregulare is characteristic of transgressive
shoreface sandstones in the Qilakitsoq
Member, especially at Qilakitsoq and
Nuuk Killeq. For location, see Fig. 2.
The marine delta front association comprises coarsening-upward
units where mudstones with marine fossils
deposited below storm-wave base are overlain by
heterolithic mudstones and sandstones which pass up
into shallower water facies. These units are interpreted
as the result of delta front progradation of shelf deltas.
The distributary channel association consists of crossbedded,
medium- to coarse-grained sandstones, which
are interpreted as having been deposited within almost
straight to slightly sinuous fluvial channels (Olsen 1991,
1993). Small fluvial channels are included in the delta
plain association, which is characterised by carbonaceous
mudstones, sandstones and coal beds, interpreted as having
formed through vertical aggradation of subaerial to
freshwater lacustrine or swamp deposits on the lower
and upper delta plain. The coal beds are interpreted as
the in situ accumulations of plant remains in both freshand
brackish-water environments. The transgressive sand
sheet association includes thin beds of sand with erosive
bases and often with numerous marine trace fossils, indicating
deposition on a marine shoreface (G.K. Pedersen
& Rasmussen 1989; Midtgaard 1991; Olsen 1991; Olsen
& Pedersen 1991; G.K. Pedersen & Pulvertaft 1992;
G.K. Pedersen & Bromley 2006). The erosional bases represent
ravinement surfaces.
Boundaries. The lower boundary of the Qilakitsoq
Member is not exposed. The upper boundary, which
corresponds to the upper boundary of the Atane For -
mation, is everywhere an erosional unconformity. Dif -
ferent units overlie the member throughout the region;
these include the Itilli, Kangilia, Quikavsak and
Atanikerluk Formations as well as volcanic rocks of the
Vaigat Formation (Fig. 16).
Geological age. The geological age of the Qilakitsoq
Member is Middle Turonian to Santonian at Ataata Kuua,
Coniacian at Alianaatsunnguaq (Birkelund 1965), San -
tonian − earliest Campanian at Paatuut, Nuuk Killeq
and on central Nuussuaq (Koch 1964; Boyd 1990, 1992;
Olsen & Pedersen 1991; G.K. Pedersen & Pulvertaft
1992; Nøhr-Hansen 1996; D.J. McIntyre, personal communication
1997). Stable carbon isotopes in wood fragments
suggest a Middle to Late Santonian age (Ambirk
2000).
Correlation. The Qilakitsoq Member correlates with part
of the Itilli Formation (western Nuussuaq and Svartenhuk
Halvø).
Subdivision. The Qilakitsoq Member includes the Itivnera
Bed in the Aaffarsuaq valley near Tunoqqu.
Itivnera Bed
revised bed
History. The Itivnera beds were described by Dam et al.
(2000) as fluvial sandstones incised into the top of the
Qilakitsoq Member (Atane Formation) at two widely
separated localities: Itivnera and Ataata Kuua (Figs 40,
82). The erosional, lower boundary was interpreted as a
sequence boundary. At Itivnera, the fluvial deposits are
80

Fig. 63. Type locality of the Itivnera Bed in
central Nuussuaq (for location, see Fig.
82). The bed comprises three channellised
sandstone units up to 38 m thick that cut
down into Santonian deltaic deposits of the
Qilakitsoq Member (Atane Formation).
The Itivnera Bed is overlain by submarine
fan deposits of the Itilli Formation
(Aaffarsuaq Member). The sandstone cliffs
are about 16 m high and the spacing
between the valleys is less than 100 m (see
Dam et al. 2000).
m
15
10
5
0
cl si sand pb
Fig. 64. Type section of the Itivnera Bed. Neither the base nor the
top of the fluvial sandstone unit is exposed (from Dam et al. 2000).
For legend, see Plate 1; for location, see Fig. 82.
overlain by deep marine deposits belonging to the
Aaffarsuaq Member of the Itilli Formation. At Ataata
Kuua, a valley incised into the Atane Formation is filled
by turbidite mudstones, sandstones and conglomerates
referred to the late Maastrichtian to earliest Paleocene
Kangilia Formation; the Itilli Formation is not present
at Ataata Kuua (Figs 14, 15, 16). The Qilakitsoq Member
here is of Turonian–Santonian age. Fine-grained organicrich
sediments preserved in the top of a small fluvial
channel contain palynomorphs indicating a Coniacian
age.
The fluvial channel deposits at Ataata Kuua that were
previously referred to as Itivnera beds are now assigned
to the Qilakitsoq Member on the basis of photogrammetric
mapping (A.K. Pedersen et al. 2007b) and dating
of the fine-grained channel fill, which lies within the
age range of the Qilakitsoq Member at this locality. The
presence of Early Campanian fluvial deposits at Ataata
Kuua cannot be demonstrated.
The Itivnera beds sensu Dam et al. (2000) constituted
the basal part of the Itilli Formation. In the present paper,
this unit is restricted to the cemented channel sandstones
at Itivnera which are defined here as the Itivnera Bed of
the Qilakitsoq Member.
Name. The strata are named after the saddle feature
named Itivnera between Nalluarissat and Tunoqqu (Fig.
82). The name was derived from a nearby locality shown
on the geodetic map from 1966 (Geodætisk Institut
1966); the spelling has not been changed to modern
Greenlandic orthography because the locality is not
shown on later geodetic maps.
81

Type section. The strata exposed on the south-facing slope
of Nalluarissat between Aaffarsuaq and Kangersooq, just
west of Itivnera, are designated as the type section (Figs
63, 64). The type section is located at 70°29.50´N,
53°08.87´W.
Distribution. The bed has only been recognised on the
south-facing slope of Nalluarissat between Aaffarsuaq
and Kangersooq (Fig. 82).
Thickness. The bed is up to 38 m thick and confined to
lensoid bodies up to 100 m wide.
Lithology. The bed consists of cross-bedded coarse-grained
sandstones, arranged in fining-upward successions form
lensoid bodies arranged like pearls on a string (Figs 63,
64). Basement pebble conglomerates are locally present.
The sediments between the cemented sandstone bodies
are covered by scree (Dam et al. 2000).
Fossils. Macrofossils have not been found.
Depositional environment. The sandstones of the Itivnera
Bed were deposited in fluvial channels (Dam et al. 2000).
Boundaries. The Itivnera Bed erosively overlies deltaic
deposits of the Qilakitsoq Member (Atane Formation).
In the type section, the fluvial sandstones are succeeded
by turbiditic mudstones and sandstones of the Aaffarsuaq
Member (Itilli Formation). The lower boundary is no
longer interpreted as a sequence boundary because there
is insufficient evidence that a sea-level fall preceded the
rise in sea level that marks the transition to the deep-water
deposits of the Aaffarsuaq Member.
Geological age. At Nalluarissat, just west of Itivnera, the
Qilakitsoq Member is Late Santonian in age, and at
Tunoqqu, immediately east of Itivnera, the Aaffarsuaq
Member is of Early to Middle Campanian age (Nøhr-
Hansen 1996). Deposition of the fluvial sandstone bodies
at Itivnera is therefore well constrained to the Early
Campanian.
Formation is here extended to include the unnamed
Upper Turonian to Campanian marine strata on
Svartenhuk Halvø and Nuussuaq (cf. Birkelund 1965;
Henderson et al. 1976; J.G. Larsen & Pulvertaft 2000).
Furthermore, on northern Disko at Kussinerujuk and
Asuk, outcrops previously correlated with the Paleocene
Kangilia Formation (J.M. Hansen 1980b; Pulvertaft &
Chalmers 1990) are here assigned to the Itilli Formation
(see below). The Itivnera beds of the Itilli Formation
(Dam et al. 2000) are, however, now redefined as the
Itivnera Bed of the Qilakitsoq Member (Atane For -
mation).
On Itsaku (Svartenhuk Halvø), the ?Upper Campa -
nian/Maastrichtian to Paleocene succession has been suggested
to be equivalent either to both the Itilli and Kangilia
Formations (i.e. Campanian to Paleocene) or to the
Kangilia Formation alone (i.e. upper Maastrichtian to
Paleocene), based on correlation of two major conglomerate
horizons with tectonic events recognised on
Nuussuaq (J.G. Larsen & Pulvertaft 2000). Based on
zircon provenance data, this succession is here assigned
to the Kangilia Formation (see below).
Name. After Itilli, a major valley transecting Nuussuaq
from north-west of Marraat on the south coast to west
of Niaqornat on the north coast (Figs 2, 65).
Distribution. The Itilli Formation is exposed in the Itilli
valley (Fig. 65) and on the north coast of Nuussuaq in
the ravines between Ikorfat and Niaqornat (Fig. 74)
where it has been drilled in the shallow wells GGU
400705, GGU 400706, and GGU 400407 (Chri stiansen
et al. 1994a), and the formation is probably also present
in the FP94-11-02, FP94-11-04 and FP94-11-05 wells
(Dam & Nøhr-Hansen 1995). It is also well exposed on
central Nuussuaq along the slopes of the valley of
Aaffarsuaq between Qilakitsoq and Tunoqqu, along the
slopes of the valley Kangersooq (Fig. 82), and in the valley
of Agatdalen including the shallow well GGU 400702
(Fig. 113; Nøhr-Hansen 1996; Dam et al. 2000). On
Disko, the formation is exposed at Asuk and Kussinerujuk.
Itilli Formation
new formation
History. The strata exposed in river sections in the Itilli
valley on western Nuussuaq were informally assigned to
the Itilli formation by J.M. Hansen (1980b). The Itilli
Facing page:
Fig. 65. Map of the southern part of the Itilli valley showing outcrops
of the Itilli Formation (Anariartorfik Member) and the Eqalulik
Formation and location of the wells Marraat-1, GANW#1, GANE#1,
GANK#1 GRO#3 and FP94-9-01. Based on Rosenkrantz et al.
(1974) and Hald (1976). Contour interval 200 m. For location, see
Fig. 2.
82

782
Quaternary cover
54°
888
Maligât Formation
Vaigat Formation
FP94-9-01
Eqalulik Formation
Undifferentiated Cretaceous–
Paleocene deposits
Itilli Formation
Ice
1084
Sermersalik
Qaasersut
1088
Sea/lake
Fault
Well
l e
U k a
r s a lik
I l u
g i s
s o
r s u
a q
795
P i n g u n n g u u p K u u a
I t i l l i
A n
a
r
i
a
t o
k
r f i
830
Gassøen
Marraat Killit
1136
GANW#1
Vaigat
Marraat-1
70°30’
Niaqornaarsuk
Kuussuaq
Eqalulik
GANE#1
GANK#1
5 km
GRO#3
Contour interval 200 m
Nuusaq
83

The Itilli Formation is also exposed in the eastern part
of the Svartenhuk Halvø area (Fig. 73; J.G. Larsen &
Pulvertaft 2000) where it was cored in the Umiivik-1
well (Dam et al. 1998b).
On Nuussuaq, the lower part of the formation (Early
Campanian and older) is only present west of the
Kuugannguaq–Qunnilik Fault (Chalmers et al. 1999
fold-out 2) where it is exposed in the Itilli valley area. In
this area, the formation was cored in the FP94-9-01 (Fig.
65; Madsen 2000) and GANT #1 wells (Fig. 74; Dam
1996a).
Type section. The type section of the Itilli Formation is
located in the southern part of the Itillli valley along the
Pingunnguup Kuua river and its tributaries, Ukalersalik
and Anariatorfik (Figs 65, 66, Plate 2). The type section
was described briefly by J.M. Hansen (1976, 1980a) and
in detail by Dam & Sønderholm (1994). Neither the base
nor the top of the formation is exposed in the type section.
The base of the type section is located at 70°36.35´N,
54°13.79´W.
Reference sections. Reference sections showing the lower
boundary with the Atane Formation are exposed at
Kussinerujuk and Asuk on the north coast of Disko (Figs
55, 77) and in the Aaffarsuaq valley on central Nuussuaq
(Fig. 83). The upper boundary towards the Kangilia
Formation is located on the north coast of Nuussuaq
around Kangilia (Figs 72, 74, 87; Birkelund 1965;
Rosenkrantz 1970; Henderson et al. 1976). The upper
boundary towards the Eqalulik Formation is exposed at
Qilakitsoq on central Nuussuaq (Figs 82, 83).
Well reference sections are available from the fully
cored boreholes FP94-9-01 (Madsen 2000), Umiivik-1
(Dam 1997), and GANT#1 (Dam 1996a). The formation
was drilled but not cored in the GRO#3 well (Fig.
67; Kristensen & Dam 1997). For details on these wells,
see below under description of members.
Thickness. The formation is more than 1400 m thick at
the type locality where the base and top of the formation
are not exposed (Plate 2). In the nearby GRO#3 well,
the formation is more than 2000 m thick (Fig. 67). The
formation thins dramatically eastwards across the
m
800
750
700
650
600
550
500
Not exposed (dyke)
Not exposed
Fig. 66. Expanded sedimentological log showing a representative
portion of the Itilli Formation in the type section along the
Pingunnguup Kuua river; the entire section, at a smaller scale, is
shown in Plate 2. For legend, see Plate 1; for location, see Fig. 65.
From Dam & Sønderholm (1994).
470
mud
sand
pebbles
84

Kuugannguaq–Qunnilik Fault and is only 240 m thick
along the northern slopes of the Aaffarsuaq valley between
Qilakitsoq and Tunoqqu. At Kangilia, on the north coast
of Nuussuaq, the formation is at least 250 m thick (Fig.
87), and the nearby GANT#1 well penetrated 645 m of
the formation without reaching the base of the formation.
On Svartenhuk Halvø, the drilled and cored part
of the formation is 960 m thick (excluding twenty-two
Paleocene dolerite intrusions with a total thickness of
240.2 m), but the base of the formation was not reached
(Fig. 75). At Kussinerujuk on the north coast of Disko,
the measured part of the formation is 42 m thick (Fig.
77; Pulvertaft & Chalmers 1990).
Series Stage Strat.
Paleocene
Danian
Vaigat Fm
Eqalulik
Fm
Agatdal Fm
m
100
200
300
400
500
600
700
GRO#3
0
GR
300
240
DTC
40
Submarine
canyon
Lithology. In the type section, the Itilli Formation comprises
mudstones, thinly interbedded sandstones and
mudstones, chaotic beds, amalgamated beds of coarsegrained
to very coarse-grained sandstone, and giant-scale
cross-bedded sandstones (Figs 66, 68, 69, 70, Plate 2; Dam
& Sønderholm 1994). These lithological contrasts are
reflected in the blocky pattern in the petrophysical logs
of the GRO#3 well (Fig. 67; Kristensen & Dam 1997).
In the Aaffarsuaq area, the Itilli Formation comprises
mudstones, thinly interbedded sandstones and mudstones,
and amalgamated sandstone and conglomerate
units together with chaotic beds comparable to those in
the Itilli valley (Dam et al. 2000). The main differences
between the Itilli and Aaffarsuaq areas are that most of
the channellised amalgamated sandstone and conglomerate
units in Aaffarsuaq are separated from the underlying
deposits by major erosional surfaces or minor
angular unconformities and that they are generally coarsergrained
than their Itilli counterparts. Furthermore, the
chaotic beds in Aaffarsuaq occur at many levels in the
section and are not restricted to a position immediately
underlying a channellised sandstone unit, and the
interbedded sandstone and mudstone units often show
an overall thinning-upward trend.
The amalgamated sandstone and conglomerate units
of the Aaffarsuaq area consist of very coarse- to mediumgrained
sandstone and conglomerate beds grading upward
into thinly interbedded sandstones and mudstones. These
coarse-grained units are up to 50 m thick, extend laterally
beyond the extent of outcrop (several hundred metres)
Upper Cretaceous
No palynomorphs recorded due to thermal influence
Campanian lower Maastricht. upper Maastricht.
Con.
Kangilia Fm
Itilli Formation
Anariartorfik Member
800
900
1000
1100
1200
1300
1400
1500
1600
1700
1800
1900
2000
2100
2200
2300
2400
2500
2600
2700
2800
Submarine
canyon
Slope
2900
Fig. 67. Lithological log of the GRO#3 well interpreted from petrophysical
data. GR, Spectral gamma-ray log; DTC, Sonic log; Con.,
Coniacian; Maastricht., Maastrichtian; Strat., lithostratigraphy;
T.D., total depth. Modified from Christiansen et al. (1999). For
location, see Fig. 65.
3000
T.D.: 2996 m
Hyaloclastite
Intrusion
Mudstone
Sandstone
85

Fig. 68. Outcrop of the Itilli Formation in
the type locality in the Anariartorfik gorge
showing amalgamated sandstones and
thinly interbedded sandstones and mud -
stones (prominent sandstone unit is
approxi mately 30 m thick). Anariartorfik
section 930–1010 m (Plate 2). For
location, see Fig. 65.
Fig. 69. Thinly interbedded sandstones and
mudstones of the Itilli Formation in the
Anariartorfik section (1070–1150 m; Plate
2). For location, see Fig. 65.
Fig. 70. Amalgamated sandstones of the
Itilli Formation (Anariartorfik Member)
deposited from turbidity currents in slope
channels overlying contorted mudstones
(at river level). Pingunnguup Kuua section
460–510 m (Plate 2). The amalgamated
sandstone unit is approximately 30 m thick
and is cut by a dyke. For location, see Fig. 65.
86

and include clasts of intraformational mudstone, sandstone
(probably derived from the underlying Atane For -
mation), redeposited concretions and basement lithologies.
On the north coast of Nuussuaq and on Svartenhuk
Halvø, the formation is dominated by mudstones, thinly
interbedded sandstones and mudstones, and bioturbated
thinly interbedded sandstones and mudstones. These
lithologies are arranged in coarsening-upward successions
10–50 m thick (Fig. 75).
At Kussinerujuk on the north coast of Disko, the formation
consists of sandstones and conglomerates with
angular cobbles and boulders of mudstone, sandstone,
or interbedded sandstone and mudstone. Other clasts consist
of rounded pebbles of quartz and clay ironstone (Fig.
77; Pulvertaft & Chalmers 1990, fig. 6). At Asuk, the
formation consists of a basal sandstone or conglomerate
bed succeeded by sand-streaked mudstones (Fig. 55).
Fossils. Ammonites, belemnites, inoceramid bivalves (Fig.
71) and rare crustaceans and corals are present in the
formation at several localities on Nuussuaq and
Svartenhuk Halvø (Birkelund 1965; Rosenkrantz 1970;
Dam et al. 2000). However, most of these are not found
in situ in the outcrops and may furthermore be reworked
intraformationally or derived from older deposits.
Dinocysts, spores and pollen occur throughout in small
numbers but cannot be determined neither in the lower
part of the Umiivik-1 and GRO#3 wells nor from the
outcrops in the Itilli valley. Burrows are occasionally present
at the top of sandstone beds. Details of fossil contents
are presented under the description of individual
members.
Depositional environment. The Itilli Formation was primarily
deposited in slope and submarine fan environments.
In the type area the amalgamated sandstones were
deposited in slope channels initiated during sea level
lowstands whereas the mudstones and the thinly interbedded
sandstones and mudstones were deposited in interchannel
slope areas (Dam & Sønderholm 1994). Details
on the depositional environment are presented under
the description of individual members.
Boundaries. On the north coast of Nuussuaq, the Itilli
Formation overlies the Atane Formation in a small and
poorly exposed section at high altitude immediately east
of the Ikorfat Fault (Fig. 22; A.K. Pedersen et al. 2006b).
The boundary with the underlying Atane Formation is
well exposed on central Nuussuaq along the northern slope
of the Aaffarsuaq valley between Qilakitsoq and Tunoqqu
(Fig. 82; Nøhr-Hansen 1996; Dam et al. 2000) and on
northern Disko at Kussinerujuk and Asuk (Fig. 2). In
Aaffarsuaq, the lower boundary is placed at the unconformity
between the Santonian deltaic deposits of the
Atane Formation and the first turbidite sandstone or
mudstone deposits of the Campanian Aaffarsuaq Member
(Fig. 83). At Kussinerujuk and Asuk, the lower boundary
is an erosional unconformity between the deltaic
deposits of the Atane Formation and the slope deposits
of the Itilli Formation (Figs 55, 77, 78, 79).
The upper boundary is well exposed on northern
Nuussuaq where it is defined at a major unconformity
with the upper Maastrichtian – Lower Paleocene Anner -
tuneq Conglomerate Member of the Kangilia Formation
(Figs 72, 76, 87). However, in areas outside the distri -
bution of the Annertuneq Conglomerate Member, there
28 cm
Fig. 71. Giant inoceramid bivalves on top
of a turbidite sandstone bed of the Itilli
Formation (Aaffarsuaq Member) in the
second ravine east of Qilakitsoq. For
location, see Fig. 82.
87

Kangilia
Formation
Fig. 72. Unconformity between the Itilli
Formation (Umiivik Member) and the
overlying Kangilia Formation with the
resistant pale-weathering Annertuneq
Conglomerate Member at the base. North
coast of Nuussuaq, at Annertuneq. Base of
conglomerate is at c. 300 m a.s.l. For
location, see Fig. 74.
Itilli
Formation
is no lithological contrast at the boundary between the
Itilli and Kangilia Formations and in these areas bio -
stratigraphic data may be essential for the distinction
between the Turonian to lower Maastrichtian Itilli
Formation and the mainly Danian Kangilia Formation.
On Svartenhuk Halvø, the formation is overlain by hyaloclastite
of the Vaigat Formation or, as observed on the
east slope of Firefjeld, by a conglomeratic unit that may
be correlated with either the Agatdal Formation or with
the Quikavsak Formation. The upper boundary of the
Itilli Formation is not exposed on northern Disko.
On the north coast of Nuussuaq and in the GANT#1
and GRO#3 wells, the Itilli Formation is unconformably
overlain by the Kangilia Formation (Figs 67, 72, 87).
Along the Aaffarsuaq valley, the upper boundary is
ambiguous and can be difficult to identify. East of
Qilakitsoq, however, Campanian deposits of the Itilli
Formation are overlain by a Paleocene conglomerate/sandstone
unit referred to the Eqalulik Formation (Fig.
83) thus indicating a major unconformity. At Nassaat,
a tributary on the south-eastern side of Agatdalen, the
presence of Upper Santonian mudstones with Sphenoceramus
was reported by Rosenkrantz (1970); this succession
is now referred to the Itilli Formation. At this
locality, the mudstones are overlain by pebbly sandstones
and bituminous mudstones, a unit that referred to the
Agatdal Formation by Rosenkrantz (1970 fig. 4c) but to
the Upper Atanikerdluk Formation (Quikavsak Formation
of this paper) by Koch (1959 fig. 37). No new data are
available from this outcrop.
Geological age. A ?Late Turonian to early Maastrichtian
age range for the formation is indicated by the ammonite
fauna (Fig. 16). Palynomorph data are generally in accordance
with the ammonite data, but local discrepancies
occur, probably due to redeposition of ammonites from
the underlying deposits.
At Asuk and Kussinerujuk on northern Disko, the
Itilli Formation is of Cenomanian–Turonian age (Fig. 16;
Bojesen-Koefoed et al. 2007) whereas on Svartenhuk
Halvø, the formation is of Turonian to Early Campanian
age (Fig. 16; Nøhr-Hansen 1996, unpublished data;
Dam et al. 1998b). Strata of Campanian age referred to
the Hilli Formation are also exposed on Nuussuaq (Itilli,
Aaffarsuaq, Agatdalen; Birkelund 1965; Sønderholm et
al. 2003). The Maastrichtian part of the formation is
only known from Kangilia and Aaffarsuaq (Birkelund
1965; Rosenkrantz 1970; Nøhr-Hansen 1996) and has
been dated in the GRO#3 well (Sønderholm et al. 2003).
Detailed information on the age of the various members
is found in the description of the members below.
Correlation. The pre-Early Campanian part of the formation
is coeval with the Atane and Upernivik Næs For -
mations (Fig. 16).
Subdivision. Four members are recognised, the
Anariartorfik, Umiivik, Kussinerujuk, and Aaffarsuaq
Members, of which the Anariartorfik Member is found
only west of the Kuugannguaq–Qunnilik Fault. The
Anariartorfik Member consists of interbedded turbidite
channel sandstones and mudstones deposited in a faultcontrolled
slope environment. The Umiivik Member is
the northernmost representative of the Itilli Formation.
It is finer grained than the Anariartorfik Member, and
dominated by major coarsening-upward successions
88

deposited in a base-of-slope and basin-floor fan environment.
Both the Anariartorfik and Umiivik Members
record deposition from probably the Cenomanian to the
Maastrichtian. The Kussinerujuk Member is only exposed
on northern Disko at Asuk and Kussinerujuk and represents
a Cenomanian transgressive event on top of the
Atane Formation. The Aaffarsuaq Member crops out
east of the Kuugannguaq–Qunnilik Fault on central
Nuussuaq and comprises a relatively thin wedge of Lower
to Middle Campanian strata that are distinctly different
from the Anariartorfik Member with regard to their large
content of intraformational clasts, the overall lack of
fine-grained mudstones and the lenticular shapes of the
thinly interbedded sandstone and mudstone units. The
sediments of the Aaffarsuaq Member were deposited in
a deep marine, channellised footwall fan system.
Anariartorfik Member
new member
History. Strata referred here to the Anariartorfik Member
were described informally as the Itilli Formation by J.M.
Hansen (1980b). Detailed studies of strata assigned to
the Anariartorfik Member were published by Dam &
Sønderholm (1994) and Madsen (2000).
Name. The member is named after the Anariartorfik valley
leading into the Itilli valley (Fig. 65).
Distribution. The Anariartorfik Member is exposed in the
Itilli valley and is present in the subsurface west of the
Kuuganguaq–Qunnilik Fault in the western part of
Nuussuaq (Fig. 11).
Type section. The type section is the same as for the Itilli
Formation in the southern part of the Itilli valley (Figs
65, 66, Plate 2). The base of the type section is located
at 70°36.35´N, 54°13.79´W.
Reference sections. Well-exposed reference sections are
located in the northern part of the Itilli valley and in the
adjoining Tunorsuaq valley (Figs 2, 65, 74).
The member was cored in the FP94-9-01 borehole
between 32 and 522 m in the central part of the Itilli valley
(Fig. 65; Madsen 2000); the cores are stored at GEUS
in Copenhagen. The member was drilled but not cored
in the GRO#3 well between 959 m and 2996 m (Figs
65, 67; Kristensen & Dam 1997).
Thickness. The member has a thickness (including intrusions)
of at least 2037 m in the GRO#3 well. Approxi -
mately 1400 m are exposed in two incomplete sections
in the Itilli valley (Fig. 65, Plate 2).
Lithology. In the type section, the Anariartorfik Member
is dominated by mudstones and thinly interbedded sandstones
and mudstones, chaotic beds, amalgamated beds
of coarse-grained to very coarse-grained sandstones, and
giant-scale cross-bedded sandstones (Figs 66, 68, 69, 70,
Plate 2; Dam & Sønderholm 1994). These lithological
contrasts create a characteristic blocky pattern in the
petrophysical log of the GRO#3 well (Fig. 67; Kristensen
& Dam 1997).
The mudstones are dark grey to black, show parallel
lamination and occur in intervals up to 15 m thick in
the type section. Persistent layers of early diagenetic
ankerite concretions occur in most mudstone intervals.
The thinly interbedded sandstone and mudstone units
comprise laterally extensive graded laminae and beds of
fine- to very coarse-grained sandstone capped by parallel-laminated
mudstones; this facies forms successions
several tens of metres in thickness (Plate 2). The sandstone
beds range in thickness from less than 1 cm to 80
cm, have flat, locally scoured bases and show normal
grading; the beds may be structureless near their base or
may be parallel- or cross-laminated throughout. The
sand stone beds are laterally persistent at outcrop scale
(> 100 m) and there is generally no systematic variation
in thickness. Convolute bedding and slump structures
are common. Early diagenetic ankerite concretions are
common in the mudstone units.
The chaotic beds are up to 30 m thick and consist of
contorted, laminated mudstone, thinly interbedded sandstone
and mudstone, and homogenised mudstone with
scattered sand grains, reworked early diagenetic ankerite
concretions, semi-indurated mudstone and sandstone
clasts and occasional basement clasts. The chaotic beds
invariably underlie a thick unit of amalgamated sandstone
beds and are often associated with sandstone dykes (Fig.
66, Plate 2).
The amalgamated sandstone beds form up to 50 m
thick channel-shaped bodies that can be followed for
1–2 km along strike (Figs 66, 68, 70, Plate 2). The sandstone
units are erosionally based and locally show welldeveloped
flute casts and channel-shaped scours at the
base. The sandstone units may show a thinning-upward
trend and have a gradational or sharp, but non-erosional
contact to the overlying interbedded sandstone and mudstone
units. Internally, the sandstone units are dominated
by amalgamated, normally graded, medium-grained
89

■
■
■
■
■
54°
Quaternary cover
Svartenhuk Formation
Uparuaqqusuitsut
Vaigat Formation
Intrusion
■
400709
Kangiusap Im a
Eqalulik Formation
400708
■
■
■
Quikavsak/Agatdal Formation
■
■
■
■ ■
■
■
■
Firefjeld
■
■
400712
■
■ ■
■
■
Umiiviup Kangerlua
■
Umiivik-1
400710
400711
■
■
■
■
■
■
Itsaku
■ ■
■
Fig. 37
Fig. 36
Qeqertarsuaq
■
66
■
■
■
■
Kangilia Formation
Itilli Formation
Umiivik Member
Upernivik Næs
Formation
Precambrian basement
Ice
Sea/lake
Normal fault
(tick on downthrow side)
Major fault with variable sense
of movement through time
Monoclinal flexure
■ ■
■
■
■
■
■
■
Karrat
Fjord
71°30'
Drill hole
■ ■
■ ■
■ ■
■
■
10 km
Fig. 73. Geological map of the south-eastern part of Svartenhuk Halvø and the west coast of Qeqertarsuaq showing the location of the
Umiivik-1 well (type section of the Umiivik Member of the Itilli Formation) and the position of shallow wells drilled by GGU in 1992 (GGU
400708–400712). Reference sections of the Upernivik Næs Formation on Qeqertarsuaq are indicated (see Figs 36, 37). For location, see Fig. 2.
Modified from J.G. Larsen & Grocott (1991) and J.G. Larsen & Pulvertaft (2000).
to pebbly, very coarse-grained sandstone beds (0.1–3.5
m thick) or, less commonly, show planar and trough
cross-bedding. The graded beds have planar, erosional
bases and can be followed laterally for more than 140 m
without major variations in thickness (Figs 66, 68, 70).
Angular mudstone clasts, ranging from a few millimetres
to 45 cm across and rounded basement pebbles up
to 8 cm across are common in the graded beds. In some
cases, the uppermost part of the graded sandstone beds
show well-developed parallel lamination, with parting lineation
and tool marks, trough cross-bedding, low-angle
cross-bedding and climbing ripple lamination. The graded
sandstone beds are commonly separated by thin mudstone
beds or units of thinly interbedded mudstone and
sandstone.
Giant-scale cross-bedded sandstone units occur as
channel-shaped bodies at a few levels in the type section.
The units comprise 7–15 m thick low-angle, crossbedded
sets dominated by coarse- to medium-grained
sandstone; the sets can be followed for approximately
150 m in a dip direction. At one locality, a single set fills
out a large channel-shaped erosional depression that is
approximately 300 m wide (Plate 2 at 800 m; Dam &
Sønderholm 1994).
Fossils. Macrofossils have not been found in this member,
but burrows are locally present at the top of the
sandstone beds. They include common Ophiomorpha
isp., Thalassinoides isp., escape burrows, and rare Helminthopsis
isp. (Dam & Sønderholm 1994). Identifiable
palynomorphs are very rare in the area of the type sec-
90

VK
53°30’ 53°15’
Niaqornat
Tupersuartaa
Hamiteskløft
Iterlaa
Serfat
Niaqorsuaq
FP94-11-05
22
18 400707 Annertuneq
Saviaqqat
Kangilia
400706
FP94-11-04
FP94-11-02
400705
3
70°45’
U i n g a
j a a
Tunorsuaq
DR
r s u a q
1290
6
5
Danienkløft
GANT#1
Quaternary cover
Ice
Tunorsuaq
Vaigat Formation
Sea/lake
Intrusion
Strike and dip of strata
Eqalulik Formation
Drill hole
Kangilia Formation
with AC Member
Itilli Formation,
Umiivik Member
Abandoned settlement
2500 m
Fig. 74. Geological map of the north coast of Nuussuaq showing outcrops of the Itilli and Kangilia Formations. The wells FP94-11-02, -04 and -05 are located near Serfat. The
shallow wells drilled by GGU in 1992 (GGU 400705–400707) are located at Annertuneq. The GANT#1 well is in the Tunorsuaq valley. DR, Danienrygge; AC, Annertuneq
Conglomerate Member. Contour interval is 200 m. For location, see Fig. 2. Modified from Rosenkrantz et al. 1974.
91

tion, but are abundant in the cuttings from the middle
and upper part of the GRO#3 well (Nøhr-Hansen 1997c).
Depositional environment. Deposition of the Anariartorfik
Member took place in a fault-controlled slope environment
(Dam & Sønderholm 1994). Most of the channellised
amalgamated turbidite sandstone beds were
deposited from high-density turbidity currents in confined
low-sinuosity channels, although a few examples
of giant-scale, cross-bedded sandstones are interpreted as
the products of lateral accretion in meandering slope
channels.
The thinly interbedded sandstones and mudstones
are interpreted as having been deposited from traction
currents and from fall-out processes associated with various
sedimentation stages within waning low-density
currents. The lateral continuity and the lack of systematic
vertical thickness variations in the thinly interbedded
sandstones and mudstones suggest that these deposits
were not confined by channel-levee systems, but most
likely represent interchannel slope deposits.
Where present, the chaotic beds always underlie undisturbed
channel sandstones. This suggests that the channels
were initially excavated by retrogressive slumping of
unstable sediments on the slope followed by channel
excavation by scouring (Dam & Sønderholm 1994).
Boundaries. The lower and upper boundaries of the
Anariartorfik Member are not exposed. The upper boundary
was drilled in the GRO#3 well but not cored (Fig.
67). An erosional unconformity between the Anariartorfik
Member and the overlying Kangilia Formation was suggested
by Kristensen & Dam (1997).
Geological age. Palynomorphs in the GRO#3 well indicate
a ?Coniacian/Santonian – early Maastrichtian age
for the uppermost c. 525 m of the Anariartorfik Member.
In the lowermost 1510 m of the well, the organic material
is degraded due to thermal maturation and this part
of the formation cannot be dated (Nøhr-Hansen 1997c).
Umiivik Member
new member
History. Outcrops of marine Upper Cretaceous strata
referred to the Umiivik Member on Svartenhuk Halvø
and northern Nuussuaq have only been briefly described
by earlier workers since their main focus was on the collection
of fossils (Rosenkrantz et al. 1942; Birkelund
1956, 1965; Rosenkrantz 1970). Later studies in connection
with mapping by the Geological Survey and
drilling of stratigraphic wells in the Umiivik area of
Svartenhuk Halvø have been reported by Christiansen
(1993), Dam et al. (1998b), Christiansen et al. (2000)
and J.G. Larsen & Pulvertaft (2000). On northern
Nuussuaq, extensive stratigraphic studies have been carried
out at Annertuneq and Kangilia (Christiansen et al.
1992; Christiansen 1993; Christiansen et al. 1994) and
at Serfat in connection with drilling of mineral exploration
wells (Dam & Nøhr-Hansen 1995).
Name. The member is named after the stretch of shore
located south-east of Firefjeld in the inner part of the
Umiiviup Kangerlua bay, eastern Svartenhuk Halvø (Fig.
73).
Distribution. On Svartenhuk Halvø, the Umiivik Member
is locally exposed in the north-western part of the peninsula
(Fig. 2), and more extensively in the low-lying coastal
outcrops around the bay of Umiiviup Kangerlua, and c.
5 km north-west of the south-eastern corner of the peninsula
(Fig. 73). On Nuussuaq, exposures are found along
the north coast between Niaqornat and Ikorfat and in
the Tunorsuaq valley (Figs 2, 74).
On Svartenhuk Halvø, the member has been cored in
five shallow wells (GGU 400708–712; Christiansen
1993; Christiansen et al. 1994a) and in the deep Umiivik-
1 well (Fig. 73; Christiansen et al. 1994; Nøhr-Hansen
1996; Christiansen et al. 1997; Dam 1997; Nøhr-Hansen
1997a; Dam et al. 1998b).
On the north coast of Nuussuaq the member has been
penetrated in six shallow boreholes: GGU 400705–707
and FP4-11-02, FP94-11-04 and FP94-11-05 (Chri -
stiansen et al. 1994; Dam & Nøhr-Hansen 1995), and
in the deep GANT#1 well (Fig. 74; Christiansen et al.
1996c; Dam 1996a; Dahl et al. 1997; Nøhr-Hansen
1997b; Kierkegaard 1998).
Type section. The most complete section of the member
is available in the Umiivik-1 core drilled on the southern
shore of Umiiviup Kangerlua on Svartenhuk Halvø
(GGU 439301; Figs 73, 75). Neither the base nor the
top of the member is, however, seen in this well. The cores
are stored at GEUS in Copenhagen. The Umiivik-1 well
is located at 71°36.70´N, 54°02.52´W.
Reference sections. The best-exposed outcrops of the
Umiivik Member are found below the Kangilia Formation
(Annertuneq Conglomerate Member) at Annertuneq
and Kangilia on the north coast of Nuussuaq (Figs 72,
92

Umiivik-1
m
Overburden
★
★
No palynomorphs recorded due to thermal influence from igneous intrusions
900
1000
1100
★
★ ★
★ ★
★
★
★
?Upper Turonian
500
600
700
★
★
Upper Coniacian
Upper Turonian – ?Upper Coniacian
100
200
300
★
★
★
★
★
Upper Turonian
★
400
★
1200
clay si vf
fmcvc
sand
800
clay si
vf fmcvc
clay si vf fmcvc
sand
sand
★
Fig. 75. Sedimentological log showing type section of the Umiivik Member (Itilli Formation) in the Umiivik-1 well. For location, see Fig.
73; for legend, see Plate 1. Modified from Dam et al. (1998b).
87). At Annertuneq, the GGU cores 400705–707 were
drilled to supplement the outcrop studies (Fig. 74;
Christiansen et al. 1994). In the GANT#1 well, the interval
from 255.8 m to 900.6 m (Fig. 76) is assigned to the
Umiivik Member (Dam 1996a). The cores are stored at
GEUS in Copenhagen.
Thickness. The total thickness of the Umiivik Member
is unknown, but in the Umiivik-1 well on Svartenhuk
Halvø it is at least 960 m thick (excluding a total of 22
dolerite intrusions with a cumulative thickness of 240.2
m). In the slopes behind the Umiivik-1 drill site, approximately
185 m of poorly exposed mudstone is present
below the base of the hyaloclastic volcanic rocks of the
Vaigat Formation – this part of the succession is partly
penetrated by the cores 400710–711 (Fig. 73; Christiansen
et al. 1994). In the GANT#1 well, on northern Nuussuaq,
620 m have been cored (excluding intrusions).
Lithology. The Umiivik Member is dominated by black
mudstones intercalated with laminae and thin beds of
sandstone; carbonate concretions are common (Figs 75,
93

310
610
m
GANT#1
Overburden
350
50
650
400
100
700
Itilli Formation
Umiivik Member
750
Itilli Formation
Umiivik Member
450
500
Kangilia Formation
Annertuneq Conglomerate Member
150
200
800
550
250
850
Itilli Formation
Umiivik Member
600
300
900
clay si vf f mcvc f mc
sand pebbles
clay si vf f mcvc f mc
sand pebbles
clay si vf f mcvc f mc
sand pebbles
94

76). Heavily bioturbated interbedded sandstones and
mudstones, chaotic beds, and structureless, muddy sandstones
also occur. Indistinct thickening- and coarseningupward
cycles, 2–85 m thick, can be seen in the Umii -
vik-1, FP94-11-02 and FP94-11-04 wells (Fig. 75; Dam
& Nøhr-Hansen 1995). A cobble conglomerate composed
of lithified sandstone clasts in a mudstone matrix is
exposed in stream gullies on the south side of Uparu -
aqqusuitsut on north-eastern Svartenhuk Halvø (Fig.
73; Christiansen et al. 2000).
In the GANT#1 core, chaotic beds, muddy sandstones
and sandy mudstones alternate with thick, sharpbased
fining-upward successions (Fig. 76; Dam 1996a).
The fining-upward successions consist of amalgamated
sandstone beds grading upward into thinly interbedded
sandstones and mudstones. Thin coarsening-upward successions
also occur. The amalgamated sandstones consist
of normally graded, medium- to coarse-grained
sandstone beds with scattered basement pebbles and
mudstone intraclasts. The sandstone beds are generally
structureless, but parallel and cross-lamination occurs
towards the top of some beds. A thin mudstone layer usually
caps the sandstone beds.
The thinly interbedded sandstones and mudstones
consist of sharp-based, graded laminae and beds of finegrained
to very coarse-grained sandstone alternating with
black parallel-laminated mudstones. The sandstones are
well-sorted and may show parallel and cross-lamination;
small mudstone rip-up clasts frequently occur throughout
the sandstone beds.
Fossils. Ammonites from the Umiivik Member have been
described from several localities on Svartenhuk Halvø
and include Scaphites mariasensis umivikensis (Birkelund),
Scaphites preventricosus svartenhukensis (Birke lund),
Clioscaphites sp. aff. saxitonianus (McLearn), Scaphites
cobbani (Birkelund), Scaphites rosenkrantzi (Birkelund),
Scaphites cf. corvensis (Cobban), Clioscaphites saxitonianus
septentrionalis (Birkelund), ammonites of the genus
Haresiceras and inoceramids of the steenstrupi group
(Birkelund 1965). Belemnites from Svartenhuk Halvø
Facing page:
Fig. 76. Sedimentological log of the Umiivik Member (Itilli Formation)
and the Annertuneq Conglomerate Member (Kangilia Formation)
in the GANT#1 well. For location, see Fig. 74; for legend, see Plate
1. Modified from Dam (1996a).
include Actinocamax cf. primus (Arkhangelsky) and
Actinocamax sp. (Birkelund 1956). Unidentified teleost
fish remains have also been found in strata yielding
Coniacian ammonites (Bendix-Almgreen 1969).
Ammonites occur at several localities along the north
coast of Nuussuaq in the Umiivik Member, including
Pseudophyllites skoui (Birkelund), Scaphites (Hoploscaphites),
S. (H.) greenlandicus (Donovan), S. (H.) ravni (Birkelund),
and S. (H.) ikorfatensis (Birkelund). The belemnites
Actinocamax groenlandicus (Birkelund) and Actinocamax
aff. groenlandicus (Birkelund), and an indeterminate solitary
corallum have also been collected (Birkelund 1956,
1965; Floris 1972).
Dinocysts are abundant in the Umiivik Member (Dam
& Nøhr-Hansen 1995; Nøhr-Hansen 1996, 1997a;
Dam et al. 1998b).
Depositional environment. The Umiivik Member records
deposition from low-density and high-density turbidity
currents, debris flows, slumping and fall-out from suspension.
Deposition of the mudstones and intercalated
mudstones and sandstones took place in a base-of-slope
and basin-floor fan environment. The succession in the
GANT#1 well, which is situated close to the Kuugan -
guaq–Qunnilik Fault, reflects a fault-controlled base-ofslope
environment with major and minor distributary
feeder channels, small turbidite lobes and interdistributary
channel areas.
Boundaries. The Umiivik Member unconformably overlies
the Atane Formation on the north coast of Nuussuaq
in a small and poorly exposed section at high altitude
immediately east of the Ikorfat Fault (Fig. 22; A.K.
Pedersen et al. 2006b).
West of the Ikorfat Fault, the lower boundary of the
Umiivik Member is not exposed and has not been drilled.
On northern Nuussuaq, the member is unconformably
overlain by the Kangilia Formation (Figs 72, 74, 87). At
most localities on Svartenhuk Halvø, it is unconformably
overlain by Paleocene hyaloclastic rocks of the Vaigat
Formation (Fig. 73). At Firefjeld, however, a thin Paleo -
cene conglomeratic unit that may be correlated with
either the Agatdal Formation or the Quikavsak Formation
is present between the Umiivik Member and the volcanic
succession.
Geological age. The age of the Umiivik Member is based
on dinocyst and ammonite data (Birkelund 1965; Nøhr-
Hansen 1996, 1997a). The ammonites from Svartenhuk
Halvø indicate a ?Late Turonian – Early Campanian age
for the Umiivik Member in this area (Fig. 16). Dinocysts
95

from the Umiivik-1 well indicate a ?Late Turonian – Late
Coniacian age for the uppermost 659 m of the well;
below this palynomorphs are not preserved due to severe
alteration of the mudstones by the Paleocene dolerite
intrusions. It is likely, however, that the core includes
Cenomanian–Turonian strata (Nøhr-Hansen 1997a;
Dam et al. 1998b). Dinocysts from outcrops and from
the three shallow wells (GGU 400710, 400711, 400712)
along the southern shore of Umiiviup Kangerlua on
Svartenhuk Halvø indicate a Santonian to Early Cam -
panian age (Nøhr-Hansen 1996).
On the north coast of Nuussuaq, the ammonites indicate
the presence of Upper Campanian and Maastrichtian
strata which is in accordance with palynostratigraphic dating
(Birkelund 1965; Nøhr-Hansen 1996).
m
50
40
Solifluction, volcanic scree
Poorly exposed
Kussinerujuk Member
new member
History. On northern Disko at Kussinerujuk and Asuk,
local outcrops of conglomerate, sandstone and mudstone
unconformably overlying the Atane Formation
have previously been correlated with the Paleocene
Kangilia Formation (J.M. Hansen 1980b; Pulvertaft &
Chalmers 1990). Later, these beds were included in the
Asuup Innartaa Member of the Danian Quikavsak
Formation (Dam 2002). On the basis of new biostratigraphic
data, however, these are here assigned to the
Kussinerujuk Member of Cenomanian–Turonian age
(Bojesen-Koefoed et al. 2007).
Name. The member is named after Kussinerujuk on the
north coast of Disko, where it is exposed in narrow gorges
(Fig. 2).
Distribution. The member is only known from the north
coast of Disko around Kussinerujuk and Asuk.
Type section. The type section of the member is in the
ravines at Kussinerujuk (Figs 2, 77, 78). The type section
is located at 70°13.10´N, 53°27.68´W.
Itilli Formation
Kussinerujuk Member
Atane Formation
Kingittoq Member
30
20
10
Fig. 77. Type section of the Kussinerujuk Member (Itilli Formation)
at Kussinerujuk, north coast of Disko. For location, see Fig. 2; for
legend, see Plate 1. Base of section is c. 450 m a.s.l.
0
vf f m c vc
clay silt sand
pebbles,
cobbles
96

Fig. 78. Type locality of the Kussinerujuk
Member (Itilli Formation) at Kussinerujuk.
Note the basal erosional boundary with the
Atane Formation beneath; the uppermost
depositional unit underlying the Kingittoq
Member is a dark grey, delta front
mudstone. The Kussinerujuk Member is
dominated by mud-clast conglomerates
with a matrix of sand (see Fig. 77). For
location, see Fig. 2.
Itilli Fm
Kussinerujuk Mb
Atane Fm
Kingittoq Mb
3 m
Reference sections. Reference sections are found in the
coastal cliffs east of Asuk (Figs 55, 79). The lithologies
here differ from those of the type section but are locally
affected by complicated deformation resulting from landslides
obscuring the stratigraphic relationships (Bojesen-
Koefoed et al. 2007).
Thickness. At Kussinerujuk the measured part of the formation
is at least 42 m thick (Fig. 77; see also Pulvertaft
& Chalmers 1990) but the member may be up to a couple
of hundred metres thick.
Lithology. The Kussinerujuk Member comprises thinly
interbedded mudstones and sandstones, and mudstone
clast conglomerates, first described by Pulvertaft &
Chalmers (1990 fig. 6).
At Kussinerujuk the member consists of mud-clast
conglomerates of varying thicknesses, with angular clasts
of cobble to boulder size, interbedded with medium- to
coarse-grained sandstone (Fig. 77). In some conglomerate
beds, the clasts are imbricated whereas other conglomerates
appear to be disorganised. Pebble-sized clasts
consist of rounded quartz and clay ironstone while angular
cobbles and boulders consist of mudstone, sandstone,
or interbedded sandstone and mudstone.
At Asuk, the Atane Formation is overlain by mudstones
and sandstones that are referred to the Kussinerujuk
Member. These sediments occur in three separate outcrops.
The westernmost of these is seen in Fig. 79, the
central outcrop is seen in Fig. 80, and the eastern is seen
in the coastal cliff adjacent to the huge alluvial fan at
Qorlortorsuaq. The western outcrop is overlain by volcanic
breccias and lavas of the Asuk Member (lower part
of the Vaigat Formation; Bojesen-Koefoed et al. 2007).
The volcanic rocks are part of a major landslide, and the
complicated relationships seen in Fig. 79 suggest that
the sediments at this locality are also affected by sliding;
their stratigraphic relationships with the central and eastern
outcrops are thus uncertain.
A simplified sedimentological log from the central
outcrop is shown in Fig. 55. Here a basal conglomerate
of mudstone and sandstone clasts in a matrix of coarsegrained
sand erosionally overlies the Atane Formation and
is succeeded by parallel-laminated sandstones interbedded
with sand-streaked mudstones (Figs 55, 80).
The western, landslipped outcrops comprise a unit of
parallel-laminated, sand-streaked mudstone, locally with
small-scale load structures (Fig. 81A). Other units consist
of strongly erosional, channellised sandstones that cut
into mudstones (Fig. 81 B); thicker sandstone beds are
fine- to medium-grained and show parallel lamination
and ripple cross-lamination. Other sandstone beds are
structureless and have erosional bases with sole-marks.
Fossils. Brackish to marine dinocysts occur in the member
and are relatively abundant at Asuk (McIntyre 1994a,
b) noted that rich pollen and spore assemblages dominated
by bisaccate conifer pollen are present in the type
section whereas dinocysts are very rare.
Depositional environment. The Kussinerujuk Member
records a transgressive event on top of a variably incised
97

E
W
Vaigat Formation
Asuk Member
Atane Formation
Kingittoq Member
Itilli Formation
Kussinerujuk Member
Fig. 79. Outcrops of the Itilli Formation at the western end of the coastal cliff section at Asuk. Outcrops of the Atane Formation are seen farthest
to the east (left); for detail, see Fig. 57. The pale sandstones (centre-left) are impregnated with hydrocarbons (see Bojesen-Koefoed et al.
2007).The dark grey mudstones in the centre of the photograph are referred to the Kussinerujuk Member as are the sandstones to the west.
The dark-weathering rocks cropping out above these sandstones are referred to the volcanic Asuk Member (Vaigat Formation). These volcanic
rocks are part of a major landslide, and the complicated structural relationships between the pale sandstones and the mudstones of the
Itilli Formation suggest that the coastal exposures may be affected by landslides. The height of the cliff is c. 30 m. For location, see Fig. 2.
surface capping the Atane Formation east of the
Kuuganguaq–Qunnilik Fault. The genetic relationships
between the two outcrop areas of the member are, however,
poorly understood. The conglomerates at the type
locality at Kussinerujuk were deposited from channellised
sediment gravity flows at unknown water depths possibly
generated by slope failure in a deeply incised channel.
Farther east, at Asuk and Qorlortorsuaq, the mudstonedominated
succession is tentatively interpreted to be
deposited in a marine environment during transgression.
Deposition occurred below storm wave base on a
gently sloping sea floor from low-energy unconfined turbidity
currents or distal storm-generated flows.
Boundaries. The lower boundary, as exposed at
Kussinerujuk, Asuk and Qorlortorsuaq (Fig. 2), is an
erosional unconformity where mudstones or mud-clast
conglomerates sharply overlie deltaic sandstones of the
Atane Formation (Kingittoq Member; Figs 16, 55, 77).
The upper boundary is not exposed, but is probably an
erosional unconformity overlain by Paleocene hyaloclastite
breccias of the Vaigat Formation.
Geological age. Spores, pollen and dinocysts indicate a
Cenomanian to Late Turonian age for the member at
Kussinerujuk (McIntyre 1994a, b; this study). Dinocysts
indicate a Cenomanian age at Asuk (Fig. 16; Bojesen-
Koefoed et al. 2007).
Itilli Fm
Kussinerujuk Mb
Atane Fm
Kingittoq Mb
Fig. 80. Erosional unconformity between
the Atane Formation and the Itilli Forma -
tion (see Fig. 55) in the coastal cliff east of
Asuk. The coastal cliff is c. 30 high. For
location, see Fig. 2.
98

A
B
Itilli Formation
Kussinerujuk Member
Fig. 81. A: Silt-streaked mudstone with small-scale load structures in the Kussinerujuk Member (Itilli Formation) at Asuk. Lens cap for scale.
B: Land-slipped deposits of erosionally based sandstones interbedded with mudstones at Asuk are assigned to the Kussinerujuk Member of
the Itilli Formation. Encircled persons for scale; for location, see Fig. 2.
Correlation. The Kussinerujuk Member is coeval with
parts of the Umiivik and Anariartorfik Members of the
Itilli Formation.
Aaffarsuaq Member
new member
History. The un-named Upper Cretaceous marine sandstones
and shales exposed on central Nuussuaq that were
informally referred to the Aaffarsuaq member by Dam
et al. (2000), are mainly known for the remarkable discoveries
in 1952 of huge specimens of Upper Santonian
– Lower Campanian inoceramid (Sphenoceramus) bivalve
shells (Fig. 71; Rosenkrantz 1970).
Name. The member is named after the Aaffarsuaq valley
on central Nuussuaq (Fig. 82).
Distribution. The member is found on central Nuussuaq
where it is well exposed along the south-facing slopes of
Aaffarsuaq between Qilakitsoq and Tunoqqu. Minor
exposures are present in a stream section on the northfacing
slope of Aaffarsuaq, south of Nalluarissat, in
Kangersooq (Fig. 82) and in Turritelladal at Scaphites -
næsen, and in Agatdalen where the Teltbæk fault crosses
the Agatdalen river (Figs 82, 113; Dam et al. 2000).
Type section. The type section is located in the second ravine
east of Qilakitsoq on the northern slopes of Aaffarsuaq
(Figs 82, 83). The base of the type section is located at
70°28.70´N, 53°21.97´W.
Reference sections. Well-exposed reference sections occur
in ravines on the northern side of Aaffarsuaq along
Nalluarissat, between Qilakitsoq and Tunoqqu (Fig. 82).
Thickness. In the main outcrop area, the thickness of the
member decreases eastward from c. 250 m in the type
section to 65 m at Tunoqqu.
Lithology. The Aaffarsuaq Member is characterised by
amalgamated sandstone and rip-up mudstone and sandstone
clast conglomerate units alternating with thinly
interbedded sandstones and mudstones, dark, sandstreaked
mudstones, and chaotic beds of homogeneous
mudstone commonly cut by sandstone dykes and synsedimentary
faults (Figs 83, 84, 85, 86; Dam et al. 2000).
The amalgamated sandstone and conglomerate units
of the Aaffarsuaq Member consist of very coarse- to
medium-grained sandstone and conglomerate beds grading
upwards into thinly interbedded sandstones and
mudstones. These coarse-grained units are up to 50 m
thick and extend laterally beyond the extent of outcrop
(several hundred metres) or occasionally form lenticular
bodies. Individual beds have planar erosional bases and
internally show normal grading. Beds are from

500
500
Itivnera
Agatdalen
400
Quaternary cover
Ice
400
Vaigat Formation
Sea/lake
70°32'
400
Eqalulik Formation
Abraham Member
Itilli Formation,
Aaffarsuaq Member
500
Kangersooq
Atane Formation
Qilakitsoq Member
Strike and dip of strata
Contour in metres
1600
1600
900
Tunoqqu
800
700
1400
600
500
400
1400
70°31'
300
12
8
8
5
IB
Nalluarissat
8
10
13
20
79
17
30
24
27
21
Ravine 1
Ravine 2
Ravine 3
Ravine 4
Qilakitsoq
1000
800
700
600
500
53°25' 53°20' 53°15' 53°10'
53°05' 53°00'
73°30'
2 km
Aaffarsuaq
200
400
300
Fig. 82. Geological map of the north side of the Aaffarsuaq valley between Qilakitsoq and Agatdalen. The type section of the Qilakitsoq Member (Atane Formation) is located along Qilakitsoq,
and the type section of the Aaffarsuaq Member (Itilli Formation) is located in Ravine 2. IB, type section of the Itivnera Bed. Contour interval is 100 m in the sedimentary outcrops, 200 m in
the Vaigat Formation. Modified from Rosenkrantz et al. (1974).
100

160
140
120
100
Vaigat Formation
Eqalulik Fm
Abraham Mb
m
320
300
280
Volcaniclastic
sediments
Not exposed
Not exposed
Itilli Formation
Aaffarsuaq Member
80
260
240
60
Itilli Formation
Aaffarsuaq Member
220
40
200
20
180
Atane Fm
Qilakitsoq Mb
0
mud
vf f m c vc f m c
sand pebbles
mud
vf f m c vc f m c
sand pebbles
Fig. 83.Type section of the Aaffarsuaq Member (Itilli Formation), second ravine east of Qilakitsoq, compare with Fig. 85. For location, see
Fig. 82; for legend, see Plate 1. Modified from Dam et al. (2000).
101

Aaffarsuaq Mb
Itilli Fm
Fig. 84. Unconformity between Santonian
deltaic deposits of the Atane Formation
(Qilakitsoq Member) and Campanian
turbidite sandstones and conglomerates of
the Aaffarsuaq Member (Itilli Formation).
East-side of Tunoqqu. For location, see
Fig. 82.
Qilakitsoq Mb
Atane Fm
to more than 5 m thick and are commonly separated by
thin mudstone beds (Figs 83, 85). The sandstones are
mostly structureless, whereas the conglomerates show
considerable lateral variation, are poorly sorted, and
always have a coarse-grained sandy matrix. Both matrixand
clast-supported conglomerates occur. The clasts consist
of intraformational mudstone, sandstone (probably
derived from the underlying Atane Formation), concretions
and basement lithologies (Dam et al. 2000).
The amalgamated sandstone and conglomerate units
are overlain by thinly interbedded sandstone and mudstone
units with either a gradational or a sharp contact.
These units are up to 30 m thick and show a general thinning-
and fining-upward trend (Figs 83, 85). They consist
of laterally persistent, normally-graded,

Fig. 85. Mudstones and conglomeratic sandstones of the upper part of the Aaffarsuaq Member (Itilli Formation) in the type section in the
second ravine east of Qilakitsoq, see Fig. 83, c. 175–300 m. For location, see Fig. 82.
observed in the Anariartorfik Member, suggesting that
downslope failure could also be associated with seismic
activity (Dam et al. 2000).
Geological age. The ammonites at Scaphitesnæsen indicate
an Early Campanian age (Baculites obtusus Zone) for
the Aaffarsuaq Member. The mudstones are generally
almost barren of palynomorphs but a rich flora is locally
Fig. 86. Conglomerate at the top of the
type section of the Aaffarsuaq Member
(Itilli Formation); note the predominance
of sedimentary clasts. Ruler is 120 cm
long. For location, see Fig. 82.
103

present that suggest an Early–Middle Campanian age
for the member (Nøhr-Hansen 1996; Dam et al. 2000).
Boundaries. The lower boundary is an angular unconformity.
Tilted strata of the deltaic Qilakitsoq Member
(Atane Formation) were truncated during the transgression
recorded by the Aaffarsuaq Member (Dam et al.
2000). Along the Aaffarsuaq valley, the Aaffarsuaq
Member is unconformably overlain by Paleocene hyaloclastites
of the Vaigat Formation (A.K. Pedersen et al.
2002). However, in two ravines along Aaffarsuaq, it is
overlain by Paleocene mudstones and volcaniclastic sandstones
referred to the Eqalulik Formation (Figs 82, 83,
see below).
Kangilia Formation
revised formation
History. The Kangilia Formation was established by
Rosenkrantz (1970) to encompass the Danian (Lower
Paleocene) conglomerate-based, marine mudstone-dominated
succession that overlies Upper Cretaceous mudstones
(Itilli Formation of this paper) with an angular
unconformity on northern and central Nuussuaq. Based
largely on the content of fossils, he divided the formation
into four members, from base to top: the Conglo -
merate Member, a conspicuous coarse-grained, clastsupported
conglomerate unit, c. 50 m thick, the Fossil
Wood Member, comprising black mudstones with a
sandstone unit in the lower part, c. 425 m thick, the
Thyasira Member consisting of sandstones and black
mudstones with tuff beds, c. 35 m thick and the Propeamussium
Member made up of black mudstones, locally
with intercalated sandstones, c.100 m thick.
Without providing details, Rosenkrantz (in Henderson
1969 fig. 4) included the entire 300 m thick mudstonedominated
succession at Ataata Kuua (near Atâ) in the
Kangilia Formation. Furthermore, the distribution of
the Kangilia Formation was shown in a schematic section
through the Nuussuaq Basin that was presented by
Henderson et al. (1976 fig. 303). The two upper members
of the formation were also reported from Alianaat -
sunnguaq, Tupaasat and Ataa on the south coast of
Nuussuaq (Rosenkrantz 1970).
The Kangilia Formation including the basal conglomeratic
member (Annertuneq Conglomerate Member)
is formally defined here. The ‘Oyster-Ammonite Conglo -
merate’ (Birkelund 1965) is formally defined as the
Oyster–Ammonite Conglomerate Bed. The Fossil Wood,
Thyasira and Propeamussium Members are abandoned.
The strata previously assigned to the latter two are now
included in the new Eqalulik Formation (see below). On
central Nuussuaq, Dam et al. (2000) mapped a unit in
the Kangilia Formation that was informally termed the
Danienrygge member; this unit is not formally recognised
here.
On Itsaku, Svartenhuk Halvø, J.G. Larsen & Pulvertaft
(2000) suggested that the poorly dated ?Upper Cam -
panian/Maastrichtian to Paleocene succession may be
equivalent either to both the Itilli and Kangilia Formations
(i.e. Campanian to Paleocene) or to the Kangilia For -
mation alone (i.e. upper Maastrichtian to Paleocene),
on account of a tentative correlation of two major conglomerate
horizons with two discrete tectonic events
recognised on Nuussuaq. Zircon provenance data show
that the detrital zircon population of this succession has
a distinct and narrow age range peaking at 1870 Ma
whereas ages of zircons in the underlying sediments of
the Upernivik Næs Formation show a greater spread with
a distinct peak at 2750 Ma (Scherstén & Sønderholm
2007). Since there was only one major change in zircon
provenance in the section involving a shift to a unique,
single point source at the boundary between the Upernivik
Næs and the overlying deposits, the suggestion is that only
one tectonic event is recorded in the section. The entire
?Upper Campanian/Maastrichtian to Paleocene succession
on Itsaku may thus be assigned to the Kangilia
Formation.
Name. After the headland of Kangilia on the north coast
of Nuussuaq (Fig. 74).
Distribution. The formation is exposed at Ataata Kuua,
Ivisaannguit, Tupaasat, Nuuk Killeq and Alianaats -
unnguaq on the south coast of Nuussuaq (Figs 2, 6, 40;
A.K. Pedersen et al. 1993), in the northern part of Agat -
dalen on central Nuussuaq (Fig. 113), in the Tunorsuaq
valley on western Nuussuaq (where it has also been drilled
in the GANT#1 well) and along the north coast of
Nuussuaq (Fig. 74), and on Itsaku on eastern Svartenhuk
Halvø (Fig. 73). The formation has been drilled on western
Nuussuaq in the GRO#3 well (Fig. 65).
Type section. The exposures at Kangilia on the north coast
of Nuussuaq are designated as the type section (Figs 87,
88). The base of the type section is located at 70°44.90´N,
53°25.33´W.
Reference sections. Well-exposed reference sections occur
at Annertuneq (Fig. 72; Nøhr-Hansen & Dam 1997),
104

Fig. 87. Type section of the Kangilia
Formation at Kangilia on the north coast
of Nuussuaq. The log is generalised due to
intermittent exposures of the mudstone
intervals. Top of section is at Danienrygge;
for location, see Fig. 74. K/T, Cretaceous–
Palaeogene boundary. See also Figs 88 and
118. For legend, see Plate 1.
K/T
Kangilia Formation
Annertuneq Conglomerate Member
Itilli Formation
Umiivik Member
420
400
380
360
340
320
300
280
260
240
220
200
180
120
140
120
100
80
60
★
★
★
★
Poorly
exposed
Poorly exposed
vf f m c vc f m c
clay silt sand pebbl.
Submarine canyon
Unconformity
Kangilia Formation Eqalulik Formation Vaigat Fm
m a.s.l.
800
780
760
740
720
700
680
660
640
620
600
580
560
540
520
500
480
460
440
T
Poorly exposed Poorly exposed Poorly exposed
T
vf f m c vc f m c
clay silt sand pebbl.
Ataata Kuua (Figs 14, 89; Dam & Nøhr-Hansen 2001)
and at Ivisaannguit west of Ataata Kuua. The formation
was drilled and cored in the GANT#1 well in Tunorsuaq
between 35 m and 256 m (Fig. 76) and drilled in the
GRO#3 well between 728 m and 959 m (Fig. 67).
Thickness. The Kangilia Formation varies in thickness
from 440 m at Kangilia (Fig. 87) to c. 400 m at Ataata
Kuua (Fig. 15), 230 m in the GRO#3 well (Fig. 67), to
just 75 m on central Nuussuaq (H.J. Hansen 1970).
Lithology. On northern Nuussuaq the Kangilia Formation
comprises a basal approximately 85–140 m thick conglomeratic
unit overlain by a mudstone-dominated succession.
The conglomeratic unit is here formally
established as the Annertuneq Conglomerate Member.
In the lower part it is composed of amalgamated conglomerate
beds that towards the top become finer-grained
and separated by mudstone intervals (Figs 72, 76, 87; for
detailed description, see below).
The succession overlying the basal conglomerate unit
consists mainly of dark mudstones with thin beds of
fine- to coarse-grained sandstone (Figs 76, 87, 88). The
mudstones are weakly laminated; locally some of the
laminae are graded. The sandstone beds have sharp bases
and are usually normally graded. The sandstones are
structureless or parallel-laminated. Ferroan carbonate
concretions and fragments of fossil wood are common
at various levels.
105

Eqalulik Formation
Kangilia Formation
Annertuneq Conglomerate Member
Itilli Formation
Umiivik Member
Fig. 88. Outcrop of the Itilli, Kangilia and Eqalulik Formations at Kangilia. The snowline at c. 800 m corresponds roughly to the base of the
volcanic Vaigat Formation. For location, see Fig. 74.
At Ataata Kuua on the south coast of Nuussuaq, a
basal sandstone unit with scattered mudstone clasts and
transported concretions up to 1.5 m in diameter rests on
a deeply eroded surface above lowest Campanian and
older Atane Formation (Figs 14, 15). The unit forms the
base of a 107 m thick fining-upward succession; the
sandstone unit grades up into thinly interbedded sandstones
and mudstones that are capped by mudstones
with scattered basement pebbles interbedded with sandstone
lenses and layers (Fig. 89; Pulvertaft & Chalmers
1990; Dam & Nøhr-Hansen 2001). The sandstones are
largely structureless, but may grade into parallel- and
cross-laminated sandstone. Convolute bedding is developed
locally.
The sandstones occur as sheets in composite bedsets
in the basal 11 m of the succession, or as single beds that
fill wide shallow scours in the middle and upper part
(Fig. 89). The composite sandstone bedsets are succeeded
by approximately 50 m of interbedded sandstones and
mudstones consisting of sharply based laminae and beds
that grade upwards from coarse-grained to fine-grained
sandstone capped by silty mudstone (Fig. 89). These
lithologies may form sharply based fining-upward units
up to 1.5 m thick, restricted to lenticular bodies a few
tens of metres wide (Fig. 89). Erosional discordances are
common within the lenticular bodies and internally they
are made up of small amalgamated fining-upward successions.
The interbedded sandstones and mudstones are succeeded
by a 56 m thick unit dominated by massive mudstone
containing scattered sand grains and few pebbleand
cobble-sized basement clasts (Fig. 89). The mudstone
beds are interbedded with laminated mudstones with
sand streaks (Fig. 90). Conglomerates and sandstones
form an up to 40 m thick unit in the middle of the Ataata
Kuua exposure (Figs 14, 15, 89), with sedimentary facies
very similar to that seen in the prominent conglomerate
unit on the north coast of Nuussuaq. This unit is overlain
by approximately 250 m of generally poorly exposed
mudstone (Fig. 14).
106

m
150
140
130
120
110
100
90
Kangilia Formation
80
70
60
50
Fig. 90. Dark grey mudstones interbedded with thin sandstone beds
of the Kangilia Formation at Ataa (for location, see Fig. 40). The
illustrated section is c. 5 m thick.
40
Atane
Fm
30
20
10
0
clay
si
sand
pebble cobble
Just west of Ataata Kuua, several levels of coarsegrained
sandstones and conglomerates are present within
the upper mudstone succession (Fig. 91). Larger clasts
include sandstone and mudstone intraclasts, clay ironstone
concretions and kaolinised gneiss clasts. Dykes of
injected sand are also seen. Farther west these coarsegrained
levels disappear.
In Agatdalen on central Nuussuaq, the formation is
generally poorly exposed and dominated by mudstones.
A Paleocene conglomerate unit about 5 m thick was
described as the Oyster-Ammonite Conglomerate by
Birkelund (1965) and Rosenkrantz (1970). It is mainly
composed of derived, highly fossiliferous concretions
and is here formally established as the Oyster–Ammonite
Conglomerate Bed.
Fig. 89. Sedimentological log showing the lower part of the Kangilia
Formation at Ataata Kuua. Slightly modified from Dam & Nøhr-
Hansen (2001), see also Fig. 15. For location of section, see Fig. 40;
for legend, see Plate 1.
Fossils. Along the north coast of Nuussuaq, fossils are
rare in the Kanglia Formation apart from Teredo-bored
fossil wood (Mathiesen 1961; Rosenkrantz 1970). A very
107

Fig. 91. Mudstones interbedded with sandstone and channellised conglomerates (arrows point to base of conglomerate-filled channels). The
Kangilia Formation at Ataa; for location, see Fig. 40. Height of the section is c. 50 m.
small number of in situ ammonites (Hoploscaphites aff.
H. angmartussutensis) and echinoderms have been found
in a sandstone bed in the lower part of the formation and
in scattered concretions (Nøhr-Hansen & Dam 1997;
Kennedy et al. 1999). Palynomorphs are common and
are referred to five zones from the Wodehouseia spinata
Zone to the Palaeocystodinium bulliforme Zone (Nøhr-
Hansen 1997b; Nøhr-Hansen et al. 2002).
The Oyster–Ammonite Conglomerate Bed in
Agatdalen is made up of highly fossiliferous concretions
containing a mainly Maastrichtian fauna of ammonites
although concretions with Campanian and Danian species
are also present. The matrix of the conglomerate contains
Danian oysters and other bivalves, gastropods, crustaceans
and rare specimens of other fossils (Birkelund
1965; Rosenkrantz 1970).
On the south coast of Nuussuaq, fossils are very scarce
in the Kangilia Formation and only indeterminate thinshelled
bivalves and gastropods have been found in the
mudstones at Ivisaannguit. The trace fossil Planolites isp.
and escape burrows occur locally in the sandstone beds.
Depositional environment. The presence of dinocysts,
echinoderms and ammonites indicates a marine depositional
environment and the mudstones and sandstones
dominating the formation are interpreted to have been
deposited from waning, low-density turbidity currents
whereas the conglomeratic units were deposited from
108

channellised, high-density currents. Some of the mudstones
may also have been deposited from suspension.
The conglomerates and sandstones at the base of the
Kangilia Formation exhibit a characteristic suite of facies
that indicate deposition from catastrophic flows related
to high-density, turbidity currents and debris flows. On
the north coast of Nuussuaq deposition took place in a
slope environment, probably in a major submarine canyon
setting (Figs 76, 87).
At Ataata Kuua, the lower part of the formation was
deposited in a submarine canyon (Figs 15, 92) whereas
the mudstones in the upper part were deposited by dilute
turbidity currents in an unconfined slope setting. The
basal erosional unconformity represents a transverse section
through the submarine canyon (Figs 15, 92; Dam
& Nøhr-Hansen 2001). The thin lenticular fining-upward
successions are interpreted as minor turbidite channel
deposits. Dinocysts and macrofossils suggest general
marine conditions during deposition. Along the south
coast of Nuussuaq, at Ataata Kuua and Ivisaannguit, no
marine palynomorphs have been recorded (McIntyre
1993), suggesting a dominant terrestrial input.
Boundaries. The lower boundary is an erosional unconformity
that separates the Kangilia Formation from the
underlying Atane Formation on southern Nuussuaq (Fig.
15) and from the Itilli Formation on western, central
and northern Nuussuaq (Figs 14, 87, 88). Along the
north coast of Nuussuaq, in the GANT#1 and GRO#3
wells and at Ataata Kuua, the lower boundary is picked
at the base of a thick conglomerate unit that cuts down
into the underlying deposits of the Itilli and Atane
Formations. At all these localities, the lower boundary
marks the base of a major submarine canyon system (Fig.
92; Dam & Nøhr-Hansen 2001). Where the basal conglomerate
is absent, the unconformity between the Itilli
and Atane Formations is difficult to locate using lithological
criteria (mudstone overlying mudstone) and has
to be picked on the basis of biostratigraphic data.
On Itsaku (Svartenhuk Halvø), there is an angular
unconformity between the Kangilia Formation and the
underlying sediments of the Upernivik Næs Formation.
At this locality, a thick conglomerate unit occurs at the
base of the formation. Elsewhere on Svartenhuk Halvø,
the formation locally onlaps the basement or is in faulted
contact with the Umiivik Member of the Itilli Formation
(Fig. 73; J.G. Larsen & Pulvertaft 2000).
The Kangilia Formation is overlain by the Eqalulik
Formation on northern and western Nuussuaq (Figs 87,
118), the Agatdal Formation on central Nuussuaq and
possibly on Itsaku (Fig. 113), and by the Quikavsak
Formation on southern Nuussuaq (Fig. 99A).
Geological age. The dinocyst flora suggest a late Maa -
strichtian to Danian age for the Kangilia Formation on
the north coast of Nuussuaq and a Danian age in the central
part of Nuussuaq (Fig. 16; J.M. Hansen 1970; Nøhr-
Hansen 1996, Nøhr-Hansen & Dam 1997; Nøhr-
Hansen et al. 2002).
The type section of the Kangilia Formation provides
a well-exposed section across the Cretaceous–Tertiary
(K/T) boundary in a clastic, deep-water setting (Fig. 87;
Nøhr-Hansen & Dam 1997). Ammonites in the lowermost
part of the formation indicate a late Maastrichtian
age (Kennedy et al. 1999) and coccoliths indicate that
most of the section above the K/T boundary has a nanofossil
NP3–4 Zone age and consequently that NP2 and
A
B
Submarine canyon incision
Submarine canyon filling
Deltaic sandstone
Turbidite sandstone
Turbidite mud-rich heterolith
?
?
Deltaic mudstone
Clasts
Fig. 92. Conceptual model for the formation of the submarine
canyon fill of the Kangilia Formation at Ataata Kuua. From Dam
& Nøhr-Hansen (2001 fig. 4). The canyon formed in response to
listric faulting, detachment and collapse of the hanging wall (A).
The steeply dipping part of the detachment surface of the footwall
acted as the canyon wall and seems not to have been eroded to an
appreciable extent. During a subsequent transgression, the canyon
was filled with turbidite deposits (B). Colours reflect interpreted
depositional environments (see Plate 1).
109

part of the NP1 zone are probably missing or very condensed
(Nøhr-Hansen et al. 2002). The K/T boundary
was also cored by the GANT#1 well (Fig. 76).
On central Nuussuaq, Danian bivalves and gastropods
in the matrix of the Oyster–Ammonite Conglomerate
Member indicate that this part of the formation cannot
be older than Danian.
On the south coast of Nuussuaq at Ataata Kuua, palynomorphs
(mainly spores and pollen) suggest a late
Maastrichtian – Early Paleocene age for the formation
(McIntyre 1993).
Correlation. The upper, Paleocene part of the Kangilia
Formation is coeval with the Agatdal and Quikavsak
Formations (Fig. 16).
Subdivision. At the type locality of the Kangilia Formation,
the Annertuneq Conglomerate Member forms the basal
unit of the formation (Figs 76, 87). In Agatdalen, a conglomerate
unit containing abundant, derived concretions,
the so-called ‘Oyster-Ammonite Conglomerate’
of Birkelund (1965), is now formally established as the
Oyster–Ammonite Conglomerate Bed.
Annertuneq Conglomerate Member
redescribed member
History. This coarse-grained unit was established by
Rosenkrantz (1970) as the Conglomerate Member – the
basal member of the Danian Kangilia Formation in the
type section on the north coast of Nuussuaq (Figs 72,
93, 94). Rosenkrantz (1970) correlated it with his basal
Danian conglomerate in Agatdalen, a unit also referred
to as the Oyster-Ammonite Conglomerate by Birkelund
(1965) and H.J. Hansen (1970). Based on new data
from the north coast of Nuussuaq and subsurface data
from the GANT#1 well, a more thorough and formal
description is presented here. The member is retained for
the sake of continuity and also because this impressive
unit is distinctive as one of the relatively few conglomerates
in the Nuussuaq Basin.
Name. The name is derived partly from the reference
locality close to the type section and partly from its historical
name based on the lithology of the unit.
Distribution. The Annertuneq Conglomerate Member
forms a conspicuous unit along the north coast of Nuus -
suaq between Niaqorsuaq and Kangilia. It has been drilled
in the GANT#1 well in the Tunorsuaq valley (Figs 74,
76), and is assumed to be present locally in the subsurface
at the base of the Kangilia Formation.
Type section. The type section of the Annertuneq Conglo -
merate Member is the same as for the Kangilia Formation
(Figs 74, 87, 88). The base of the member is located at
70°44.54´N, 53°25.11´W.
Reference sections. A well-exposed section of the lower
part of the member is accessible in the western gully
leading to Annertuneq, a few kilometres west of Kangilia
(Figs 72, 93, 94). The member was cored in the GANT#1
well, from 256.0 m to 100.0 m (Fig. 76).
Annertuneq Conglomerate Mb
Itilli Fm
Fig. 93. The Annertuneq Conglomerate
Member (c. 40 m thick) of the Kangilia
Formation at Annertuneq. For location,
see Fig. 74.
110

Thickness. The Annertuneq Conglomerate Member varies
in thickness from c. 85 m on the north coast of Nuussuaq
(Fig. 87) to 140 m (excluding igneous intrusions) in the
GANT#1 well (Fig. 76; see also A.K. Pedersen et al.
2006b).
Lithology. At the reference section at Annertuneq, the lower
part of the conglomerate unit is composed of amalgamated
up to 8 m thick lenticular beds containing pebble- to boulder-sized
clasts up to 2 m in diameter (Fig. 94). Clasts
include quartz (40%), quartzitic grey sandstones (35%),
intraformational mudstones and concretions (10%),
quartzitic red sandstones (7%), chert (3%) and others
(5%); ‘others’ include Precambrian gneiss and granite
clasts, and clasts of silicified limestone that may be pisolitic
or contain Ordovician gastropods. The conglomerates also
include coalified wood fragments and poorly preserved
marine bivalves and gastropods. Individual conglomerate
beds can be divided into structureless, structureless
to normally graded, or inversely graded, clast-supported
conglomerate facies. The conglomerates are poorly sorted
and always contain a matrix of medium to very coarsegrained
sandstone or sandy mudstone. The sandstones
are predominantly structureless, but in some cases the
uppermost parts of the beds show well-developed parallel
lamination and cross-lamination. Dish structures and
escape burrows are common.
In the type section at Kangilia, the lower part of the
member consists of a 20 m thick unit of amalgamated
conglomerate beds comprising pebble- to boulder-sized
clasts in a poorly sorted medium- to very coarse-grained
sandstone matrix. The conglomerate units fine upwards
and sandstone becomes the dominant lithology towards
the top (Fig. 87, 95).
Fossils. Scarce, strongly worn bivalves and gastropods
and occasional, coalified wood fragments are present in
the member.
Depositional environment. Both at the type section and
in the GANT#1 well, the conglomerates were deposited
from debris flows and high density turbidite currents
and sandstones from high- and low-density turbidity
currents. It has previously been suggested that deposition
took place in a fluvial environment (H.J. Hansen
1970), but the depositional facies and inferred processes,
the upward transition into fully marine deposits and the
presence of marine dinocysts in the interbedded mudstones
(Nøhr-Hansen 1997b) indicate a marine depositional
environment. The considerable increase in the
thickness of the member in the GANT#1 well compared
Annertuneq Conglomerate Member
Itilli Formation Kangilia Formation
Fig. 94. Close-up of the sharp, erosional base of the Annertuneq
Conglomerate Member at Annertuneq. Person for scale. For location,
see Fig. 74.
to the exposures situated at Annertuneq and Kangilia, c.
6 km to the north, suggests that deposition took place
in a major submarine canyon and that the GANT#1
well is situated in a more axial position than the north
coast exposures.
Boundaries. The lower boundary of the Annertuneq
Conglomerate Member is developed as a major erosional
unconformity. On the north coast of Nuussuaq,this separates
mudstones of the Itilli Formation below from the
conglomerates of the Annertuneq Conglomerate Member
above (Fig. 72). The upper boundary is gradational at
all localities and is placed at the top of the uppermost,
very coarse-grained sandstone bed (Figs 76, 87, 93, 95).
Geological age. The Annertuneq Conglomerate Member
does not contain fossils of biostratigraphic significance.
The age of the member is, however, constrained by its
position between marine mudstones. The Umiivik Mem -
ber of the Itilli Formation (below) has a Late Campanian
111

Annertuneq
Conglomerate Member
Fig. 95. Upper boundary (dashed line) of the Annertuneq Conglomerate Member of the Kangilia Formation at Kangilia showing a gradual
transition from conglomerates and sandstones to mudstones. For location, see Fig. 74; person for scale.
age (J.M. Hansen 1980b; Nøhr-Hansen 1996, 1997b;
Dam et al. 1998c; Nøhr-Hansen et al. 2002). The mudstones
of the remaining Kangilia Formation (above) are
of late Maastrichtian – Paleocene age. The position of
the Maastrichtian–Paleocene boundary within the Kang -
ilia Formation varies between localities, from 210 m above
the base of the Annertuneq Conglomerate Member
(Nøhr-Hansen & Dam 1997), c. 70 m above the base
of the member at Kangilia (Fig. 87), to a position close
to the top of the member in the GANT#1 well (Nøhr-
Hansen 1997b). This suggests an ?early to late Maa -
strichtian age for the member.
Oyster–Ammonite Conglomerate Bed
new bed
History. In Agatdalen on central Nuussuaq, a conglomerate
of Danian age containing a huge number of derived
concretions has been referred to as the Oyster-Ammonite
Conglomerate (e.g. Birkelund 1965). H.J. Hansen (1970)
referred this conglomerate to the Thyasira Member of
Rosenkrantz (1970). For historical reasons and in order
to distinguish this fossiliferous conglomerate unit from
the Annertuneq Conglomerate Member, it is now formally
established as a bed and named the Oyster –Ammo -
nite Conglomerate Bed.
Name. The bed is named after the rich occurrence of
reworked oysters and ammonites in the conglomerate.
Distribution. The bed has only been described from three
localities in Agatdalen (Fig. 113).
Type locality. The bed is best exposed in the western river
bank of the Agatdalen river, south-east of Sill Sø (Figs
96, 113). The type locality is located at 70°34.62´N,
53°04.50´W.
Thickness. The bed is approximately 5 m thick (Rosen -
krantz 1970).
112

Fig. 96. A: Type locality of the Oyster–
Ammonite Conglomerate Bed on the
western bank of the Agatdalen river. For
location, see Fig. 113. B: Clast in the polymodal,
matrix-supported conglomerate
(paraconglomerate) in the Oyster–
Ammonite Conglomerate Bed.
Hammer (encircled) for scale.
A
See B
4 m
B
Lithology. The Oyster–Ammonite Conglomerate Bed is
a clast-supported conglomerate dominated by numerous,
calcareous concretions and dark mudstone boulders
eroded from Maastrichtian and Campanian deposits
(Fig. 96; H.J. Hansen 1970). The matrix consists of
sandy mudstone containing Danian oysters and bivalves
(see below). In places, calcareous concretions have been
formed within the conglomerate (Floris 1972).
Fossils. The fossils in the concretions are reworked and
include ammonites, oysters and other bivalves, gastropods,
crustaceans and corals (Birkelund 1965; Rosenkrantz
1970; Floris 1972). They show that the concretions were
eroded from Maastrichtian deposits and represent a rich
fauna including Hypophylloceras (Neophylloceras) groenlandicum
Birkelund 1965, Saghalinites wrighti Birkelund
1965, Baculites cf. B. meeki Elias 1933, Scaphites (Disco -
scaphites) waagei Birkelund 1965, and S. (D.) angmartussutensis
Birkelund 1965 (Hoploscaphites Nowak 1911
according to Kennedy et al. 1999). In addition Scaphites
(Hoploscaphites) cf. S. (H.) ravni Birkelund 1965, S. (H.)
cf. S. (H.) greenlandicus Donovan 1953, S. cobbani Birkelund
1965 and S. rosenkrantzi Birkelund 1965 occur very
occasionally and indicate that some concretions were
derived from the Campanian (Kennedy et al. 1999).
Corals include Stephanocyathus sp. and Caryophyllia agatdalensis
(Floris 1972). The mudstone matrix includes oysters
and other bivalves that have also been described from
the lower part of the overlying Eqalulik Formation on the
north coast of Nuussuaq (Thyasira Member of Rosenkrantz
(1970)). Dinocysts are present in both the reworked concretions
and the matrix of the conglomerate.
Depositional environment. Deposition took place from
debris flow(s) in a marine environment.
Boundaries. The lower and upper boundaries of the bed
are not well exposed. The lower boundary is inferred to
be an erosional unconformity separating the conglomerate
from underlying mudstones of the Campanian Itilli
113

Formation. The conglomerate is overlain by black bituminous
mudstones of the Kangilia Formation (Fig. 113).
Geological age. The oysters and other bivalves in the
matrix of the conglomerate indicate a Danian age (Birke -
lund 1965). The fauna has species in common with the
Thyasira Member of the Kangilia Formation of Rosen -
krantz (1970), here defined as the Eqalulik Formation,
and the conglomerate was referred to the Lower to Middle
Danian by Rosenkrantz (1970). Dinocysts from the mudstone
matrix also suggest a Danian age. Kennedy et al.
(1999) referred the ammonites to the early Maastrichtian.
The age of the Oyster–Ammonite Conglomerate Bed is
constrained by its Danian fossils and the early Late Danian
age of the Agatdal Formation, which overlies the Kangilia
Formation.
Correlation. The bed is referred to the Kangilia Formation
based on the general Danian age and the lack of volcani -
clastic material (the presence of which characterises the
Eqalulik Formation) in both the conglomerate and the
overlying mudstone.
Quikavsak Formation
new formation
History. The strata comprising the Quikavsak Formation
as defined here were briefly described by Steenstrup
(1874 p. 79) and later in detail by Koch (1959) who
included them in his Quikavsak Member of the Tertiary
Upper Atanikerdluk Formation. The strata are now established
as a separate formation. A major, fluvial channellised
sandstone unit that Koch (1959 fig. 5) previously
included in the top of the Atane Formation at Quikassaap
Kuua is now tentatively also included in the Quikavsak
Formation. At Nassaat, a tributary on the south-eastern
side of Agatdalen, a poorly exposed conglomerate unit
that had been assigned to the Sonja member (Agatdal
Formation) by Rosenkrantz (1970) and to the Quikavsak
Member by Koch (1959) is here re-assigned to the Qui -
kavsak Formation.
Dam (2002) suggested a division of the Quikavsak
Formation into four members reflecting various depositional
stages during infill and drowning of the incised
valley system. Dam’s three lower members – the Tupaasat,
Nuuk Qiterleq and Paatuutkløften Members – are defined
formally below. The Asuup Innartaa Member is no longer
recognised, and the deposits on Nuussuaq are now
included in either the Eqalulik or the Atanikerluk
Formations whereas the deposits on Disko are now
referred to the Kussinerujuk Member of the Itilli For -
mation (see below).
Name. The member is named after the stream of
Quikavsaup kûa (now spelled Quikassaap Kuua) near
Atanikerluk (Fig. 40). The spelling of the name is taken
from Koch (1959).
Distribution. The formation is exposed along the south
coast of Nuussuaq, from Nuuk Killeq in the west to
Saqqaqdalen in the east. On central Nuussuaq, the formation
is exposed at Nassaat (Fig. 2).
s
s
Atane Fm
Paatuutkløften Mb
Nuuk Qiterleq Mb
Tupaasat Mb
Quikavsak Fm
Fig. 97. The type locality of the Quikavsak
Formation, east of Nuuk Qiterleq on the
south coast of Nuussuaq (for location, see
Figs 2, 40). The Quikavsak Formation
overlies the Atane Formation and is
overlain by a very thin Eqalulik Formation
and hyaloclastite breccias of the Vaigat
Formation. A volcanic sill (S) has been
intruded between the Quikavsak and the
Eqalulik Formations. The thickness of the
Quikavsak Formation in this outcrop is c.
180 m.
114

On Svartenhuk Halvø, on the east slope of Firefjeld,
a thin (30 m) Paleocene conglomeratic unit is present
between the Itilli Formation and the hyaloclastic rocks
of the Vaigat Formation (Fig. 73; J.G. Larsen & Pulvertaft
2000). This unit may be correlated with either the Agatdal
Formation or the Quikavsak Formation.
Type section. Originally, Koch (1959) chose the exposures
at the stream of Quikassaap Kuua as the type locality
for his Quikavsak Member (Fig. 40). At this locality,
however, only two of the members of the Quikavsak
Formation are exposed (Tupaasat and Nuuk Qiterleq
Members) and the formation has an atypical appearance
(Fig. 100). The best exposures and the most complete
development of the formation occur between Paatuut
and Nuuk Killeq, south Nuussuaq. The type section is
located on the coastal slope just east of Nuuk Killeq
below the mountain Point 1580 (Figs 6, 97, 98, 99A;
A.K. Pedersen et al. 1993). The type section is located
at 70°20.75´N, 53°08.75´W.
Reference sections. Reference sections occur at Ivisaannguit,
Paatuut and Quikassaap Kuua (Figs 40, 99B, 100, 108).
Thickness. The channellised nature of the deposits forming
the Quikavsak Formation results in highly variable
thicknesses. The formation is up to 180 m thick at the
type locality. At Ivisaannguit it is up to 116 m thick, on
the west side of Ataata Kuua it is up to 135 m, on the
east side of Ataata Kuua below the mountain of Ivissussat
Qaqqaat it is more than 100 m, at Paatuut up to 162 m
and at Quikassaap Kuua it is up to 70 m thick. Between
these sections, the formation is only a few metres thick
or is absent altogether.
Lithology. Along the south coast of Nuussuaq the formation
is divided into three lithological units that are given
the rank of members (Dam & Nøhr-Hansen 2001; Dam
Quikavsak Formation
Tupaasat Mb
Nuuk Qiterleq Mb PM
m
120
110
100
90
80
70
60
50
40
30
Fig. 98. Type section of the Quikavsak Formation (and the Tupaasat
and Nuuk Qiterleq Members) at Tupaasat, east of Nuuk Qiterleq;
for location, see Figs 2, 6, 97. The upper member of the formation
(PM, Paatuutkløften Member) has not been measured at this locality.
The lenticular mud-rich body illustrated on Fig. 99A just southeast
of the section line is absent in this section, probably due to
erosion at the charred base at 39 m. Modified from Dam & Nøhr-
Hansen (2001). Note that the position of this section was erroneously
stated to be at Ivisannguit in Dam (2002). For legend, see
Plate 1.
Atane Formation
20
10
0
Kangilia Fm
Fault
clay si sand pebbles
115

NW SE
600 m.a.s.l.
Peak 1580
Tupaasat
600 m.a.s.l.
Vaigat Formation
400
Quikavsak Formation
400
Fig. 98
Paatuutkløften Mb
Nuuk Qiterleq Mb
Tupaasat Mb
Kangilia Formation
Atane Formation
200
200 400 600 800 1000 1200 1400 m
A
200
NE SW
Paatuutkløften
Vaigat Formation
750
750
m.a.s.l. m.a.s.l.
Quikavsak Formation
Paatuutkløften Mb
Nuuk Qiterleq Mb
Atane Formation
500
Tholeiitic picrite hyaloclastites
(covered by scree)
Picrite intrusives contemporary
with the Vaigat Fm
Marine mudstones (Eqalulik Fm)
Estuarine sandstones (Paatuutkløften Mb)
Fluvial sandstones (Paatuutkløften Mb)
Thin estuarine mudstones
(Paatuutkløften Mb)
0 250
Lacustrine mudstones
and sandstones (Nuuk Qiterleq Mb)
Fluvial conglomerates and
sandstones (Tupaaasat Mb)
Low-energy mudstones and sandstones
(Tupaasat Mb)
Deep marine mudstones (Kangilia Fm)
Deltaic sandstones (Atane Fm)
Tupaasat
Mb
Deltaic and pro-deltaic mudstones
and coals (Atane Fm)
Bedding planes
Fault
500 750 1000 m
B
500
116

Fig. 100. Reference locality of the
Quikavsak Formation at Quikassaap Kuua
(see Fig. 40 for location). This locality was
selected by Koch (1959) as the type locality
of his Quikavsak Member. The channellised
sandstone is now referred to the
Tupaasat Member of the Quikavsak
Formation (for explanation, see text).
20 m
Quikavsak
Formation
Atane Formation
2002). The lower, markedly erosional unit dominated by
coarse-grained sandstones succeeded by a middle unit
comprising sand- and silt-streaked mudstones and sandstones
with numerous in situ and drifted remains of trees.
The upper unit also has an erosional base and consists
of medium- to coarse-grained sandstones arranged in an
overall fining- and thinning-upward succession, locally
with a basal boulder conglomerate bed. For detailed
descriptions, see members below.
Fossils. The sandy parts of the formation are rich in coal
fragments and pieces of coalified wood. The fine-grained
parts of the formation are rich in clay ironstone with
plant fossils, sideritic silty shale with plant fossils, mostly
as impressions, and in situ coalified tree trunks. Plant fossils
belong to the ‘Upper Atanikerdluk A’ flora of Heer
(1883a, b); fossil insects and ostracods have also been
Facing page:
Fig. 99. Photogrammetrically measured sections of the incised valley
fills of the Quikavsak Formation. A: Longitudinal section of the
Tupaasat and Paatuukløften incised valleys in the area around the
type section (see Figs 97, 98). B: Cross-section of the Paatuutkløften
incised valley from Paatuutkløften (see Fig. 105). Note that the
Kangilia Formation is bounded by faults, and that the Atane Formation
is also faulted. Most of the Tupaasat Member and the Nuuk Qiterleq
Member were removed by erosion prior to deposition of the
Paatuutkløften Member. For location of sections, see Figs 2, 40.
Modified from Dam (2002; it should be noted that the figure captions
for figs 3B and 4 in this paper are switched).
described (Koch 1959). At the top of the section at
Paatuut, about 5 m below the basalts, a few marine molluscs
have been found (Koch 1959). Early Paleocene oysters
(Ostrea sp.) have been reported immediately west of
Paatuutkløften and east of Nuuk Killeq (Koch 1959).
Palynomorphs are common, but only few marine dino -
cysts are present.
Depositional environment. The Quikavsak Formation represents
fluvial to estuarine deposition in a series of faultcontrolled,
incised valley systems that formed during
two phases of uplift of the Nuussuaq Basin (Dam &
Sønderholm 1998; Dam & Nøhr-Hansen 2001; Dam
2002). The mudstone member overlying the basal sandstone
member in the type section (Fig. 98) is probably
related to a quiescent period between the tectonic events
resulting in the development of low-energy depositional
(lacustrine) areas within the valleys.
Boundaries. The lower boundary of the formation is a
major erosional unconformity formed during valley incision,
cutting at least 190 m down into the underlying
deposits (Figs 99, 109). East of Ataata Kuua, the unconformity
separates Turonian – Lower Campanian deltaic
sandstones and mudstones of the Atane Formation from
the coarse-grained deposits of the Quikavsak Formation.
The contact with the underlying Atane Formation is
generally easily recognised with the exception of the
locality at Quikassaap Kuua where the boundary relationships
are somewhat enigmatic (see below under
Tupaasat Member). On the west slope of Ataata Kuua
and westwards to Ivisaannguit and in the type section,
117

m
120
Paatuut it is succeeded by syn-volcanic lacustrine deposits
referred to the Atanikerluk Formation.
110
100
Geological age. The fauna and flora are not age-diagnostic
but a Danian age is indicated by the stratigraphic
position between the Kangilia Formation, of Danian age
on southern Nuussuaq, and the overlying Eqalulik For -
mation of Danian to Selandian age (Fig. 16; Piasecki et
al. 1992; Nøhr-Hansen et al. 2002.
Atane Formation Kangilia Formation
90
80
70
60
50
40
30
20
10
0
Fault
mud sand gravel
Quikavsak Formation
Tupaasat Member NQ
m
210
200
190
180
170
160
150
140
130
mud sand gravel
Correlation. The Quikavsak Formation deposits can be
correlated to the submarine canyon deposits of the Agatdal
Formation exposed on central Nuussuaq (Koch 1959;
Dam & Sønderholm 1998) and occurring in the subsurface
in the GRO#3 well (Fig. 67) and the GANE#1
well (Fig. 119).
Subdivision. The Quikavsak Formation is divided into
three members: the Tupaasat, Nuuk Qiterleq and
Paatuutkløften Members (Fig. 99).
Tupaasat Member
new member
History. Strata now referred to the Tupaasat Member
were first but only briefly described by Steenstrup (1874
p. 79). The member was described in detail by Koch
(1959) and referred to as the lower part of the Quikavsak
Member (Upper Atanikerdluk Formation). That part of
the section at Quikassaap Kuua described by Koch (1959
p. 17, fig. 5) as “cross-bedded quartz sandstone of a considerable
thickness” and assigned by him to the Atane
Formation, is now referred to the Quikavsak Formation
(see Fig. 100).
Fig. 101. Generalised sedimentological log from Ivisaannguit on the
south coast of Nuussuaq (for location, see Fig. 40). The sandstones
and conglomerates of the Kangilia Formation are similar to those
seen at Ataa (Fig. 91). At this locality, the Kangilia Formation has a
faulted contact with the Atane Formation and is erosionally truncated
by the Quikavsak Formation. NQ, Nuuk Qiterleq Member.
For legend, see Plate 1.
the Quikavsak Formation cuts down into mudstones of
the upper Maastrichtian – Lower Paleocene Kangilia For -
mation (Figs 14, 15, 98, 101).
West of Paatuut, the formation is overlain by marine
mudstones of the Eqalulik Formation whereas east of
Name. The member is named after the headland of
Tupaasat just west of Ataata Kuua.
Distribution. The member is exposed along the south
coast of Nuussuaq as the fill of an incised valley system
extending from Nuuk Qiterleq in the west to Saqqaqdalen
in the east where it occurs on the western slope of
Saqqaqdalen close to the Vaigat strait (Figs 40, 129; Koch
1959; Pulvertaft 1989a, b; A.K. Pedersen et al. 2007a).
The Tupaasat Member is not present in all outcrops of
the Quikavsak Formation. At some localities it was partly
or entirely eroded away prior to deposition of the
Paatuutkløften Member (see Figs 99B, 109).
118

Tupaasat Member
Atane Formation
Fig. 102. Giant-scale, cross-bedded conglomerates and sandstones of the Tupaasat Member (Quikavsak Formation). Encircled person for scale.
From the coastal slope between Tupaasat and Nuuk Qiterleq (for location, see Fig. 2).
Type section. The thickest deposits and the best exposure
of the member occur between Tupaasat and Nuuk
Qiterleq, in the coastal slope below the mountain Point
1580 (Figs 6, 98, 99, 102). This exposure is designated
as the type section. The type section is located at
70°20.75´N, 53°08.75´W.
Reference sections. There are several well-exposed sections
along the south coast of Nuussuaq, e.g. in the coastal cliffs
around Ivisaanguit (Dam 2002 fig. 4) and at Quikassaap
Kuua (Figs 40, 100).
Thickness. The member is 78 m thick in the type section,
at least 80 m at Ivisaannguit, up to 7 m in Paatuutkløften,
and c. 20 m at Quikassaap Kuua (Figs 40, 100).
Lithology. At the type locality, the lower part of the
Tupaasat Member consists of giant-scale trough cross-bedded,
parallel-bedded and structureless pebbly to cobbly,
very coarse-grained sandstone. In the lower part of the
member, each trough set is up to 30 m in thickness (Figs
98, 99, 102, 103), but set thickness decreases upwards
to less than 0.5 m at the top concomitant with a finingupward
trend; the sandstones are, however, distinctly
different from the cross-bedded medium- to coarsegrained
sandstones of the Paatuutkløften Member (Dam
2002). Pebbles are well rounded and consist of quartz
(80%), gneiss and granite (10%), metasediments (7%)
and chert (3%). Within the pebbly sandstones in the
type section area, an up to 10 m thick unit of mudstone
rich in detrital mica is intercalated with lenses of sandstone.
The mudstone is bounded at the top by an erosional
unconformity giving rise to the lenticular shape
of the shale. The shale is succeeded by cross-bedded pebbly
sandstones.
Around Ivisaannguit, the member has a similar development
to that in the type section. In the eastern part
of these exposures, the member is only up to 15 m thick.
Towards the west, the thickness of the member increases
dramatically to at least 80 m where it crosses an Early
Paleocene fault scar (Dam 2002 fig. 4).
119

In Paatuutkløften and at the spur between the coastal
escarpment and Ippigaarsukkløften, the Tupaasat Member
consists of a 7 m thin unit of pebbly, coarse- to very
coarse-grained sandstones and a pebble to cobble conglomerate
(Figs 99B, 104).
On the eastern slope of Quikassaap Kuua, a 20 m
thick set of cross-bedded medium- to coarse-grained
sandstone is present. It is well consolidated and forms a
vertical cliff (Fig. 100). This cross-bedded sandstone unit
was included in the Atane Formation by Koch (1959)
in spite of the stronger similarity to the lower part of the
Quikavsak Member farther west than to the fluvial sandstones
of the Atane Formation. This assignment may
have been based on the presence of a small unconformity,
possibly associated with a fossil podsol profile that separates
the sandstones from the overlying heterolithic
deposits, which he referred to as the Quikavsak Member
but are here assigned to the Nuuk Qiterleq Member of
the Quikavsak Formation.
Fossils. Fragments of coal and pieces of coalified wood
are common in the member.
Fig. 103. Giant-scale, cross-bedded conglomerates and sandstones
of the Tupaasat Member. Encircled person for scale. Arrows indicate
dip of major foresets. From the coastal slope above Ivisaannguit (for
location, see Fig. 40).
Depositional environment. The conglomerates and sandstones
of the Tupaasat Member form a characteristic suite
of very thick sandstone beds deposited by major bedforms
related to catastrophic flows. The flows were confined to
incised fluvial valleys formed during major tectonic uplift
of the basin (Dam et al. 1998a; Dam 2002). From the
Tupaasat Member facies alone it is not possible to determine
whether deposition took place in a subaerial or a
submarine environment. The overlying sediments, how-
Fig. 104. Tupaasat Member conglomerate
in Paatuutkløften (for location, see Fig.
99B). Hammer for scale.
120

ever, have a fluvio-lacustrine origin, which makes a subaerial
environment most likely for the Tupaasat Member.
Boundaries. The lower boundary is a major erosional
unconformity that follows the base of the incised valley
systems. It cuts across faults that bring Lower Paleocene
mudstones of the Kangilia Formation against mid-
Cretaceous deltaic deposits of the Atane Formation (Figs
98, 99A). The unconformity reflects major tectonic uplift
of the basin (Dam 2002).
Where the Nuuk Qiterleq Member is present, the
upper boundary is gradational and non-erosional (Figs
97, 98). At other localities, the Tupaasat Member is erosionally
truncated by the Paatuutkløften Member (Fig.
99).
Geological age. The Tupaasat Member is referred to the
Early Paleocene (Danian), its age being bracketed by
data from the Kangilia Formation below and the Nuuk
Qiterleq Member above (Dam 2002; Nøhr-Hansen et
al. 2002).
Nuuk Qiterleq Member
new member
History. Strata now referred to the Nuuk Qiterleq Member
are equivalent to the Quikavsak Member as described by
Koch (1959) from the type section at Quikassaap Kuua.
Moreover, the Nuuk Qiterleq Member includes the middle,
very fossiliferous unit of the Quikavsak Member
described elsewhere in the area by Koch (1959).
Name. The member is named after the headland Nuuk
Qiterleq (Fig. 2).
Distribution. The member is locally exposed along the
south coast of Nuussuaq as the fill of an incised valley
system extending from Nuuk Qiterleq in the west to
Atanikerluk in the east (Fig. 2). It is not recognised in
all outcrops of the Quikavsak Formation due to erosion
preceding deposition of the succeeding Paatuutkløften
Member.
Type section. The member is well exposed between Tupaasat
and Nuuk Qiterleq. The type section is the same as that
for the Tupaasat Member (Figs 97–99). The type section
is located at 70°20.75´N, 53°08.75´W.
Reference sections. Reference sections occur in Paatuut -
kløften and at Quikassaap Kuua (Figs 99B, 100).
Thickness. In the type section the member is 23 m thick,
at Ivisaannguit 3–6 m, at Paatuut up to 42 m and at
Quikassaap Kuua up to 50 m. The thickness is mainly
dependent on the depth of erosion into the member
prior to deposition of the overlying sandstones of the
Paatuutkløften Member (Fig. 105).
Lithology. In the type section and in Paatuutkløften, the
Nuuk Qiterleq Member is composed of up to 6 m thick
coarsening-upward successions, composed of silt- and
Paatuutkløften Member
Nuuk Qiterleq Member
Fig. 105. Nuuk Qiterleq Member erosively
overlain by the Paatuutkløften Member in
Paatuutkløften (see Fig. 99B). Helicopter
(encircled) for scale.
Atane Formation
121

Paatuutkløften
Member
Nuuk Qiterleq Member
A
B
Fig. 106. A: Thin coarsening-upward successions in the Nuuk Qiterleq Member composed of silt- and sand-streaked mudstones passing upwards
into fine- to medium-grained sandstones. Person for scale. From the type locality near Nuuk Qiterleq (for location, see Fig. 2). Arrows indicate
the location of in situ coalified tree trunks. Note the upper, sharp, erosional boundary with the Paatuutkløften Member. B: In situ vertical,
coalified tree trunk from the type section of the Nuuk Qiterleq Member. Pencil for scale (arrowed).
sand-streaked mudstones grading upward into fine- to
medium-grained sandstones (Fig. 106A). Incipient ripples
as well as wave and current ripples and parallel lamination
are widespread. In situ vertical coalified trees and
drifted tree trunks and plant fossils are very common
(Fig. 106B). At Ivisaannguit, at Paatuut and at Ippigaar -
sukkløften, the member is dominated by mudstones with
thin sand-streaks. A single, sharply based sandstone bed
occurs at Ivisaannguit.
At Quikassaap Kuua, the member consists of interbedded
siltstones and graded, occasionally parallel- laminated,
very fine-grained to very coarse-grained sandstones
(Fig. 107). This interbedded facies alternates with lenticular
beds with erosional bases consisting of normally
graded, medium- to very coarse-grained trough, crossbedded
sandstones arranged in thinning-upward successions
up to c. 50 cm thick. The interbedded siltstones
and sandstones are rich in plant fossils, clay ironstone concretions,
in situ vertical coalified tree trunks, drifted coalified
tree trunks and finely disintegrated coal fragments.
Fossils. The Nuuk Qiterleq Member is very rich in plant
fossils and contains most of the species known from the
Quikavsak Formation. The fossil flora from this member
and from the lower part of the overlying Naujât
Member (Atanikerluk Formation) at Atanikerluk and a
few additional localities is known as the ‘Upper Atani -
kerdluk A’ flora of Heer (1883a) who recognised 282
species, some of which have been revised by Brown
(1939), Seward (1939), Chaney (1951) and Koch (1963).
Koch described the Lower Paleocene flora in the Agatdalen
area where he recognised 27 species, of which 19 species
were recognised by him as also occurring in the Quikavsak
Formation.
Depositional environment. Sediments of the Nuuk Qiterleq
Member were deposited in various environments within
an incised valley system. The stacked coarsening-upward
cycles in the type section and in Paatuutkløften were
formed by repeated progradation of shoreface or bayhead
deltas into a lacustrine environment (Dam 2002).
The deposits at Quikassaap Kuua include lenticular
fining-upward successions of sandstones deposited in
minor fluvial channels, interbedded with siltstones and
graded, very fine-grained to very coarse-grained gravelly
sandstones deposited in interchannel areas. The thin
graded sandstone sheets were probably deposited during
periods of intense overbank flooding.
Boundaries. The lower boundary is placed at the lithological
change from pebbly coarse-grained sandstones of
the Tupaasat Member to the fine-grained deposits of
Nuuk Qiterleq, rich in plant fossils (Fig. 99). At most
localities, the lower boundary is non-erosional; at Qui -
kassaap Kuua, however, the Nuuk Qiterleq Member
overlies an erosional surface (Koch 1959).
122

etween Tupaasat and Nuuk Qiterleq and on central
Nuussuaq at Nassaat (Koch 1959 fig. 37). The strata
were described in detail by (Dam et al. 1998a; Dam &
Sønderholm 1998; Dam 2002).
Name. The member is named after the Paatuutkløften
ravine (Fig. 40).
Distribution. The Paatuutkløften Member is exposed
along the south coast of Nuussuaq as the fill of an incised
valley system, exposed from Nuuk Qiterleq in the west
to Ippigaarsukkløften in the east and also at Nassaat on
central Nuussuaq (Figs 2, 40).
Type section. The eastern slope of Paatuutkløften (Figs 99B,
105, 108). The base of the type section is located at
70°15.27´N, 52°40.65´W.
Reference sections. Reference sections occur on the western
slope of Ippigaarsukkløften (Figs 108, 109), at
Ivissussat Qaqqaat on the east side of Ataata Kuua (Fig.
110), in the south-west-facing cliffs above the west side
of Ataata Kuua (Fig. 14) and between Tupaasat and Nuuk
Qiterleq below the mountain Point 1580 (Figs 6, 97, 98,
99; A.K. Pedersen et al. 1993).
1 m
Fig. 107. Interbedded siltstones and sandstones of the Nuuk Qiterleq
Member on the western slope of Quikassaap Kuua (for location, see
Fig. 40). This section was previously the type section of the Quikavsak
Member of Koch (1959).
At most localities, the upper boundary is with the
Paatuutkløften Member (Figs 99, 106). At Quikassaap
Kuua, the member is overlain by dislocated (landslipped)
mudstones of the Atanikerluk Formation (Koch 1959).
Geological age. All the plants are interpreted as Danian in
age (Koch 1963).
Paatuutkløften Member
new member
History. Strata now referred to the Paatuutkløften Member
were first described and figured as the Quikavsak Member
by Koch (1959) along the south coast of Nuussuaq in
the Paatuut area (Koch 1959 figs 20–25), the Ataata
Kuua area (Koch 1959 figs 26–30) and at the localities
Thickness. The member is 145 m thick in the type section.
Thicknesses in the reference sections are 158 m at
Ippigaarsukkløften, more than 110 m at Ivissussat
Qaqqaat, 110 m in the coastal cliffs above Ataata Kuua,
up to 25 m at the coastal section above Ivisaannguit and
78 m in the section between Tupaasat and Nuuk Qiterleq.
The exposures at Nassaat are too poor to estimate the
thickness of the member.
Lithology. At Ivissussat Qaqqaat and Ataata Kuua the
member is initiated by conglomerates composed of gneiss
pebbles and boulders (Fig. 110). This is followed by
monotonous successions of light grey, well-sorted, dominantly
planar cross-bedded, medium- to very coarsegrained
pebbly sandstones that are present at all localities
(Fig. 111). These are distinctly different to the succession
characterising the Tupaasat Member (Dam 2002).
There is a general overall upward decrease in grain size,
clast size and set thickness; thin mudstone beds are occasionally
present in the uppermost part of the member.
Coal clasts, finely disseminated coal fragments and sideritic
mudstone clasts are common. Penecontemporaneous
deformation structures are widespread in some beds.
Along the south coast of Nuussuaq between Nuuk
Qiterleq and Ippigaarsukkløften, the sandstones become
123

Eqalulik Fm
m
150
140
Paatuutkløften
150
Ippigaarsukkløften
m
Fig. 108. Type and reference sections of the
Paatuutkløften Member at Paatuutkløften
and Ippigaarsukkløften, respectively (for location,
see Fig. 40; for legend, see Plate 1). The
dashed lines indicate correlative surfaces
between the two sections.
130
140
Terminal lobe
120
130
110
120
100
110
Quikavsak Formation
Paatuutkløften Member
90
80
70
100
90
80
60
50
70
60
Hydrothermal fracture
40
50
30
40
20
30
10
20
Atane Fm
0
cl si sand pebbles
Base of incised valley
10
0
cl si sand pebbles
124

Vaigat Formation
sill
Quikavsak Formation
Atane Formation
Fig. 109. Paatuutkløften Member as exposed in the Ippigaarsukkløften section (for location, see Fig. 40). The sandstones of the Paatuutkløften
Member fill a valley incised into deltaic deposits of the Atane Formation (see Fig. 108). Thickness of valley fill is c. 180 m; the white arrow
indicates the base of the reference section shown in Fig. 108.
light orange in the upper part of the member and crossbeds
show double mud drapes and reactivation surfaces
draped by mudstone clasts. Locally the cross-bedding is
bidirectional. The sandstones frequently show convolute
bedding; coal fragments, sideritic mudstone clasts
and concretions are common. Thin mudstone beds with
plant debris and heavily bioturbated sandstones occur in
the upper part of the succession.
Fossils. Few recognisable plant fossils are present in the
mudstones of the member. On the spur between the
western slope of the Ippigaarsukkløften ravine and the
coastal slope, about 5 m below the basalts, a few Danian
marine molluscs have been found (Koch 1959). Danian
oysters (Ostrea sp.) have been found immediately west
of Paatuutkløften and east of Nuuk Killeq (Fig. 2; Koch
1959). These oysters were most probably derived from
sandstones in the uppermost part of this member. Trace
fossils are common to abundant at most localities in the
upper part of the member. They include Ophiomorpha
nodosa, Ophiomorpha isp., Diplocraterion parallelum and
Thalassinoides isp. (Fig. 108).
Depositional environment. The sediments of the Paatuut -
kløften Member were deposited in an incised valley system
formed after an episode of renewed Early Paleocene
faulting. The valley system seems to follow the system
generated prior to the deposition of the Tupaasat Member,
resulting in considerable or in some cases complete erosion
of the earlier deposits within the incised valleys.
Deposition of the lower part of the member took place
in a fluvial environment during a period of rapidly rising
sea level, high river discharge and high sedimentation
rates (Koch 1959; Dam & Sønderholm 1998; Dam
2002). The upper part of the member is characterised
by a change in colour, by sedimentary structures typical
of tidal activity and by intense bioturbation, indicating
a change to a tidal estuarine environment during infilling
of the valleys (Dam & Sønderholm 1998).
125

Paatuutkløften
Member
Fig. 110. Basal gneiss-clast conglomerate of
the Paatuutkløften Member at Ivissussat
Qaqqaat (east slope of Ataata Kuua; for
location, see Fig. 40). Person for scale.
Atane Formation
Boundaries. An erosional unconformity separates the
sandstones of the Paatuutkløften Member from the underlying
incised valley deposits of the Nuuk Qiterleq or
Tupaasat Members (Figs 97, 99, 105). In some cases,
the Paatuutkløften Member is incised directly into the
Kangilia or Atane Formations suggesting either that the
previous deposits within the valley system were completely
eroded away or that new valleys were eroded
locally (Figs 14, 99, 109, 110). The sandstones of the
Paatuutkløften Member are abruptly overlain by mudstones
of the Eqalulik Formation (Figs 108, 112).
Geological age. The age of the Paatuutkløften Member is
bracketed by the Danian age of the underlying Kangilia
Formation and the latest Danian to Selandian age of the
overlying Eqalulik Formation (see p. 137), suggesting
that the age of Paatuutkløften Member is late NP3–NP4
(Nøhr-Hansen et al. 2002).
Correlation. The Paatuutkløften Member has been correlated
with marine deposits of the Agatdal Formation
on central Nuussuaq (Koch 1959; Dam & Sønderholm
1998), and with the Agatdal Formation in the GANE#1
and GRO#3 wells (Nøhr-Hansen et al. 2002).
Fig. 111. Uniformly cross-bedded fluvial sandstones of the
Paatuutkløften Member at Ippigaarsukkløften (for location, see Fig.
40). The apparent discontinuity in the middle of a section is due to
hydrothermal alteration (see Fig. 108). Encircled person for scale.
126

Fig. 112. The sharp boundary between
estuarine sandstones of the Paatuutkløften
Member and the mudstones of the
Eqalulik Formation above. Hammer (left)
for scale. From Ippigaarsukkløften (for
location, see Fig. 40).
Eqalulik
Formation
Paatuutkløften
Member
Agatdal Formation
revised formation
History. The Agatdal Formation was established by
Rosenkrantz (in: Koch 1959 pp. 75–78) to encompass
Upper Danian marine mudstones, sandstones and conglomerates
found in the Agatdalen area on central Nuus -
suaq; these sediments were further described by H.J.
Hansen (1970), Rosenkrantz (1970) and Henderson et
al. (1976). In some papers, the formation is referred to
as the Agatdalen Formation.
The Agatdalen area was the key study area for the
Nûgssuaq Expeditions led by A. Rosenkrantz because of
the rich fossil content of the sediments (see ‘Previous
work’). Focus was on the fossil assemblages, and the various
outcrops (sections) were only shown schematically
and described provisionally. The component lithological
units of the section were assigned to individual members
resulting in a complex lithostratigraphic terminology.
Four members were recognised within the small area of
outcrop: the Turritellakløft, Andreas, Sonja and Abraham
Members. Schematic sections from the localities in the
Agatdalen area are shown in Rosenkrantz (1970 figs 4,
5). The outcrops in the Agatdalen area are discontinuous,
and because many of the sandstone and conglomerate
units are channellised – and lateral facies changes
are therefore pronounced – the members are difficult to
correlate and map in detail (Figs 113, 114). A possible
correlation between the outcrops of the Agatdal Formation
is shown in Plate 3. Furthermore, the members cannot
be recognised outside the type area and therefore the
three lower members are no longer treated as formal
units. They are, however, treated as informal members
below in order to facilitate correlation between the new
data presented here and the older literature and fossil
records (see Plate 3).
The Agatdal Formation as defined here is entirely prevolcanic.
Thus, the Abraham Member, which is synvolcanic,
is now included in the new Eqalulik Formation
(see below). Rosenkrantz (1970) referred other synvolcanic
marine sediments found on Nuussuaq to the tuffaceous
Thyasira and Propeamussium Members (abandoned
here) of the Kangilia Formation. In Agatdalen, the
Turritellakløft Member, from which tuffs are not reported,
overlies the Propeamussium Member (Rosenkrantz 1970
fig. 5). The correlation between the pre- and synvolcanic
members of the Kangilia and Agatdal Formations of
Rosenkrantz is not well explained.
Strata assigned to the Agatdal Formation (Sonja
Member) at Nassaat north-east of Agatdalen (Fig. 2) by
Rosenkrantz (1970 fig. 4c, d) are here assigned to the
Quikavsak Formation, following Koch (1959). The tuffaceous
deposits of the Abraham Member are coeval with
the volcanic Asuk Member of the Vaigat Formation and
are therefore now included in the Eqalulik Formation (see
p. 137). A sandstone unit underlying the pillow breccias
at Kangilia on the north coast of Nuussuaq was tentatively
assigned to the Agatdal Formation by H.J. Hansen
(1970), Rosenkrantz (1970) and Dam & Sønderholm
(1998); this unit is regarded here as forming part of the
Eqalulik Formation.
127

1000
800
1000
53°10' 53°05' 53°00'
600
Pyramidedal
1000
26
Qaarsutjægerdal
800
600
Turritellakløft
Agatkløft
’Sonja lens’ Sill Sø
Teltbæk
70°35'
■■ ■■ ■■ ■■
Teltbæk fault
Scaphitesnæsen
I I I I I I I I I I I I
400701
400702
OA
14
800
17
600
■■ ■ ■■
Quaternary cover
Vaigat Formation
Eqalulik Formation
Agatdal Formation
Kangilia Formation
Itilli Formation,
Aaffarsuaq Member
Atane Formation
Intrusion
Agatdalen fault
12
400703
Jeepkløft
OA
14
Brayakløft
400
Agatdalen
400704
Søndre
and Nordre
Baculiteskløft
■■ ■■ ■■ ■■ ■■ ■■ ■■ ■■ ■■ ■■
600
Ice
800
Sea/lake
1000
OA exposure
14
500
Type section (OA)
Strike and dip of strata
Contour in 53°10' metres
1 km
Fig. 113. Geological map of the Agatdalen area. The positions of the four shallow wells drilled by GGU in 1992 (GGU 400701–400704)
are shown. Exposures of Oyster–Ammonite Conglomerate Bed (OA) shown with dots. From Dam et al. (2000) based on Rosenkrantz et al.
(1974). Turritellakløft is also named Turritelladal on some maps. For location, see Fig. 2.
Subsurface strata, here assigned to the Agatdal For -
mation, were first cored in the GANE#1 well drilled by
grønArctic Energy Inc. at Eqalulik on western Nuussuaq
in 1995 (Fig. 65). A thick succession of marine Paleocene
sandstones and conglomerates was drilled in 1996 by
the GRO#3 exploration well south-east of the Kuussuaq
river delta (Figs 9, 65, 67). This succession was referred
to the Quikavsak Formation by Christiansen et al. (1999),
but is here referred to the Agatdal Formation.
Name. The formation is named after the Agatdalen valley
on central Nuussuaq.
Distribution. Outcrops of the Agatdal Formation are
only known from the Agatdalen area (Fig. 113; Dam et
al. 2000). From subsurface data (GRO#3, GANE#1 and
GANE#1A wells), the formation is known also to be
present on western Nuussuaq, west of the Kuugannguaq–
Qunnilik Fault.
128

Agatdal Formation Eqalulik Formation
‘Turritellakløft
Member’
‘Andreas
Member’
Abraham
Member
Fig. 114. Type locality of the Agatdal Formation in Turritellakløft (Rosenkrantz 1970; for location, see Fig. 113). The section is approximately
80 m high. In the present paper, the Agatdal Formation is not subdivided, but the formally abandoned ‘Turritellakløft Member’ and ‘Andreas
Member’ are shown to provide a link to Rosenkrantz (1970). The Agatdal Formation is overlain by a thin development of the Abraham Member
which is part of the Eqalulik Formation. For measured section, see Plate 3 (section 1).
The Turritellakløft Member and the Abraham Member
of Rosenkrantz (1970) were described from the western
end of the Turritellakløft gorge and Qaarsutjægerdal (Figs
113–115, Plate 3; H.J. Hansen 1970), whereas the
Andreas Member was only recognised in Turritellakløft
(Figs 113, 114, Plate 3). The Sonja Member of Rosen -
krantz (1970) is only known from a section in Agatkløft,
2 km east of Turritellakløft (Figs 116, 117, Plate 3).
On Svartenhuk Halvø, on the east slope of Firefjeld,
a thin (30 m) Paleocene conglomeratic unit is present
between the Itilli Formation and the hyaloclastic rocks
of the Vaigat Formation (Fig. 73; J.G. Larsen & Pulvertaft
2000). This unit may be correlated with either the Agatdal
Formation or the Quikavsak Formation.
Type section. The type section of the Agatdal Formation
is at the so-called ‘Store Profil’ (or ‘Big Section’) in Turri -
tellakløft in the north-western end of Agatdalen (Fig.
114, Plate 3, section 1; Rosenkrantz 1970 fig. 5; Hender -
son et al. 1976 fig. 312). The type section is located at
70°35.01´N, 53°08.02´W.
Reference sections. Reference sections occur on the southern
slopes of Agatkløft and on the eastern slope of Qaar -
sutjægerdal (Figs 115, 116, 117, Plate 3).
In the subsurface, a complete section through the
forma tion was encountered in the GRO#3 well from
718 m to 423 m (Fig. 67). No cores were taken but a
complete suite of well logs is available (Kristensen &
Dam 1997). The upper part of the Agatdal Formation
was drilled and fully cored in the GANE#1A well from
706.7 m to 601.5 m (Fig. 119).
Thickness. The formation varies considerably in thickness
from 65 m in the type section to 18 m in Qaarsutjægerdal
(Plate 3). In the GRO#3 well, the formation is approximately
250 m thick (excluding igneous intrusions; Fig. 67).
129

Eqalulik
Formation
pillow breccia
Agatdal
Formation
Kangilia
Formation
Fig. 115. Thin development of the Agatdal
Formation in Qaarsutjægerdal (for
location, see Fig. 113). Sandstone beds of
the Agatdal Formation overlie mudstones
of the Kangilia Formation with marked
angular unconformity. The Agatdal
Formation is overlain by the Abraham
Member of the Eqalulik Formation. The
exposed section below the pillow breccias is
21 m thick. For measured section, see Plate
3 (section 4).
Lithology. In the Agatdalen area, the Agatdal Formation
comprises mudstones with several thick, lenticular conglomeratic
and sandstone units (Figs 114–117, Plate 3)
that Rosenkrantz (1970) had already recognised to be
partly laterally equivalent.
The Agatdal Formation, as exposed in the junction
between Agatkløft and Qaarsutjægerdal, is characterised
by a major, fining-upward succession composed of a
basal conglomerate unit grading upwards into alternating
arkosic sandstones, conglomerates and mudstones
with marine fossils and plant remains (Plate 3). The basal
conglomerate unit can be followed laterally for about 1
km, but disappears rapidly towards the south-east along
the Agatdalen river (Figs 113, 116, 117, Plate 3). The
conglomerates also seem to wedge out towards the northwest
in Agatkløft. The clasts are pebble to boulder grade
and are composed of gneiss. The conglomerates form
amalgamated beds up to 7 m thick, or alternate with
clast-rich, coarse-grained sandstones. The sandstone beds
of the overlying succession usually show normal grading
and both parallel- and cross-lamination. Sandstone streaks
are common in the mudstones interbedded with the
sandstone beds.
In the Turritellakløft section, the Kangilia Formation
is unconformably overlain by dark grey to black, sandstreaked
mudstones with sandstone lenses and sheets
which form the base of the Agatdal Formation (Fig. 114,
Plate 3; Rosenkrantz 1970). The lower part of the formation
here consists of thinly interbedded mudstones,
siltstones and sandstones. The mudstones show graded,
parallel lamination. The sandstone beds are parallel- and
cross-laminated. Trace fossils are common (J.M. Hansen
1980b).
Upwards, the sandstone beds become thicker and
occur as sheets and lenses with erosional bases. The beds
are parallel laminated or show normal grading from
coarse-grained to fine-grained sand. Locally the sandstones
are highly fossiliferous (predominantly Turritella
sp.). Intraformational mudstone and sandstone clasts are
common. Loose slabs show a preferred orientation of
Turritella shells; this parallel orientation indicates that the
shells were current-worked and may serve as palaeocurrent
indicators.
In the upper part of the Turritellakløft section is a
channellised unit of well-sorted, very coarse-grained,
tabular to wedge-shaped, cross-bedded sandstone (Fig.
114). The top of the Agatdal Formation is a 1.5 m thick
gravelly, very coarse-grained sandstone bed. Body and trace
fossils are very rare in these sandstones.
In Qaarsutjægerdal, a matrix-supported conglomerate
bed occurs at the base of the formation (Fig. 115, Plate
3). It is succeeded by well-sorted, fine- to mediumgrained
sandstones, with few mudstone interbeds. Locally
the sandstones show parallel- and low-angle cross-lamination.
Bioturbation is intense at the top of the section
where Ophiomorpha isp. and Planolites isp. are common.
The sediments are highly fossiliferous; Turritella sp. is particularly
numerous and the shells show a preferred parallel
orientation.
In the GANE#1 well, the Agatdal Formation consists
of a thick, fining-upward succession composed of a lower
sandstone unit grading upwards into a heterolithic unit.
130

Fig. 116. Basal conglomerate unit of the Agatdal Formation south of the junction between Agatdalen and Agatkløft (for location, see Fig.
113). Note how the conglomerate pinches out towards the left (south). Section is approximately 13 m high. For measured section, see Plate
3 (section 3).
The cored succession in the GANE#1 and GANE#1A
wells consists of amalgamated, thickly bedded, coarseto
very coarse-grained sandstones with normally graded
beds in places alternating with thinly interbedded sandstones
and mudstones (Fig. 119). The upper heterolithic
part of the formation consists of mudstones, thinly
interbedded sandstones and mudstones, amalgamated
sandstones grading upwards into thinly interbedded
sandstones and mudstones and muddy sandstones.
Probable scape burrows are observed locally (Dam 1996b).
Fossils. The Agatdal Formation is the most fossiliferous
of the marine units in West Greenland, with more than
500 described macrofossil species (see also ‘Previous
work’ above).
Marine fossils in the mudstones (the former Turri -
tellakløft Member) include gastropods, bivalves, scleractinian
corals, fish, ostracods, coccoliths and foraminifera
(Bendix-Almgreen 1969; Rosenkrantz 1970; Szczechura
1971; J.M. Hansen 1976; Kollmann & Peel 1983;
Petersen & Vedelsby 2000). Dinocysts are rare (J.M.
Hansen 1980b).
The sandstones of the former Andreas Member are very
poor in fossils in the Turritellakløft section, whereas certain
levels in Qaarsutjægerdal are very fossiliferous.
Turritella sp. is particularly common, but other gastropods
together with bivalves, scleractinian corals and
spines of echinoids have also been found in the member
(Rosenkrantz 1970; Floris 1972; Kollmann & Peel 1983;
Petersen & Vedelsby 2000). Wood and fragments of
leaves and fruits have been collected in this member in
Qaarsutjægerdal (Koch 1963, 1972a, b).
The sandstones and conglomerates of the former Sonja
Member are generally poor in marine fossils but locally
contain a very rich marine fauna, known mainly from
the ‘Sonja lens’. The lens was originally 7 m long and 0.7
m thick but was completely excavated by Rosenkrantz
and his co-workers. The fauna from this bed is dominated
by bivalves and gastropods, but also includes scleractinian
corals, octocorals, asteroids, crinoids, echinoids, serpulids,
brachiopods, bryozoans, scaphopods, crustaceans,
fish, foraminifera, coccoliths and palynomorphs (Bendix-
Almgreen 1969; H.J. Hansen 1970; Rosenkrantz 1970;
Szczechura 1971; Floris 1972; Perch-Nielsen 1973;
Henderson et al. 1976; J.M. Hansen 1980b; Kollmann
& Peel 1983; Collins & Wienberg Rasmussen 1992;
Petersen & Vedelsby 2000). Moreover, the Agatdal
Formation contains a well-preserved macroflora (Koch
1963). On western Nuussuaq, however, no determinable
macrofossils have been found in the Agatdal Formation.
Dinocysts are common in samples from the GRO#3
and GANE#1 wells (Nøhr-Hansen 1997b, c; Nøhr-
Hansen et al. 2002). The trace fossils Ophiomorpha isp.
and Planolites isp. are locally common (see above).
Depositional environment. In the Agatdalen area, the
macrofossils are indicative of a relatively shallow-water,
marine depositional environment, such as a lower
shoreface or inner shelf environment (Petersen & Vedelsby
2000). In contrast, the sedimentary facies are interpreted
to reflect deposition in a deep-water slope environment.
131

Fig. 117. Exposure of the Agatdal Formation in Agatkløft (for location, see Fig. 113; for measured section, see Plate 3 (section 2)). The section
is approximately 50 m high and, together with the basal conglomerate unit shown in Fig. 116, was referred to the ‘Sonja Member’ by
Rosenkrantz (1970). The completely excavated Sonja Lens was part of this section. According to H.J. Hansen (1970) the succession is capped
by 6 m of concretionary mudstone (covered by scree during the authors’ visit in 1992) underlying volcanic pillow breccias and a sill.
The mudstone-dominated units were deposited from
dilute turbidity currents in an unconfined slope setting
where the sandstone interbeds possibly represent splay
deposits from nearby submarine channels. The thick
lenticular, conglomeratic sandstones were deposited by
high- and low-density turbidite currents in submarine
slope channels. The fossils found in these units must
therefore have been transported, but probably only over
short distances, as they are not worn or fragmented.
The presence of basement boulders in the conglomerate
close to the base of the formation implies fluvial
transport from areas east of the Ikorfat fault system (A.K.
Pedersen et al. 1996 fig. 6). The conglomerates were thus
probably deposited in a submarine canyon in front of a
major delta at the mouth of the coeval incised fluvial
valley system represented by the Quikavsak Formation.
Palynological and geochemical investigations of the
GRO#3 and GANE#1 wells also indicate a marine depositional
environment (Bojesen-Koefoed et al. 1997; Nøhr-
Hansen 1997c) and the sediments record deposition
dominated by high-density turbidity currents. The thickness
of the formation in the GRO#3 and GANE#1 wells
and the overall geological setting suggests that deposition
took place in a major submarine canyon system on
a fault-controlled slope (Dam 1996b; Kristensen & Dam
1997). The small, fining-upward cycles in the upper,
heterolithic part of the canyon fill were deposited in
small turbidite channels.
Boundaries. Where the lower boundary is exposed in the
Agatdalen area the Agatdal Formation rests unconformably
on the Kangilia Formation (Figs 113, 115,
Plate 3). The Agatdal Formation is overlain by the Eqalulik
Formation (Figs 113–115, 119, Plate 3) or locally by
volcaniclastic breccias of the Vaigat Formation.
In the GRO#3 well the lower boundary is probably
an erosional unconformity separating coarse- to very
coarse-grained sandstones of the Agatdal Formation from
132

heterolithic deposits of the Kangilia Formation below
(Fig. 67). The upper boundary is placed at the base of
the reworked volcaniclastic sediments or tuffs of the
Eqalulik Formation (Fig. 67).
Age. Most fossil groups indicate a Paleocene (Late Danian)
age for the formation (Fig. 16; Bendix-Almgreen 1969;
H.J. Hansen 1970; Rosenkrantz 1970; Szczechura 1971;
Kollmann & Peel 1983; Collins & Wienberg Rasmussen
1992). The coccolith assemblage indicates a Chiasmolithus
danicus zone age (NP 3 Zone; Perch-Nielsen 1973). The
co-occurrence of the foraminifera Globoconusa daubjergensis
and Globigerina compressa indicates a P1c plankton
zone age for the Agatdal Formation (H.J. Hansen
1970; Berggren et al. 1995; Olsson et al. 1999) which
corresponds to a late NP3 – early NP4 age. In the GRO#3
well, dinocysts and nannofossils indicate an age not
younger than nannoplankton zone NP4 (Late Danian
or Early Selandian; Nøhr-Hansen 1997c; Nøhr-Hansen
et al. 2002).
Correlation. The age of the Agatdal Formation suggests
that it is coeval with the major incised valley systems of
the Quikavsak Formation on southern Nuussuaq and
with most of the upper part of the Kangilia Formation
on the north coast of Nuussuaq (Figs 11, 15, 16; Nøhr-
Hansen et al. 2002). The basal unconformity described
between the Agatdal and Kangilia Formations in the
Agatdalen area may be due to either condensation or
nondeposition of nannoplankton zones NP1 and NP2
in the type section of the Kangilia Formation.
Eqalulik Formation
new formation
History. Deposits now assigned to the Eqalulik Formation
embrace the marine synvolcanic strata below the basalts
of the West Greenland Basalt Group (Hald & Pedersen
1975) that contain volcaniclastic sandstones and tuffs.
On the north coast of Nuussuaq and on central Nuussuaq,
these strata have previously been assigned to the Thyasira
and Propeamussium Members of the Kangilia Formation
(Rosenkrantz 1970) and the Abraham Member of the
Agatdal Formation (Rosenkrantz 1970). However, the
Thyasira and Propeamussium Members are considered
inappropriate as they were established solely on the basis
of the faunal content. The use of these two members as
defined by Rosenkrantz (1970) is now abandoned and
the strata included in the new Eqalulik Formation.
On the south coast of Nuussuaq, a thin unit of marine
black shale including bioturbated sandstone beds below
the volcaniclastic breccias of the Vaigat Formation was
referred to the Asuup Inatartaa Member of the Quikavsak
Formation by Dam (2002) but is here included in the
Eqalulik Formation. Strata previously mapped as unnamed
Paleocene (Tertiary) on the north coast of Nuussuaq east
of the Ikorfat fault, in the region around the Tunorsuaq
valley, and in the Itilli and Aaffarsuaq valleys are now
assigned to the Eqalulik Formation.
Name. After Eqalulik, a lake close to the location of the
GANE#1 drill site on western Nuussuaq (Fig. 65).
Distribution. The formation is widely distributed below
the hyaloclastites of the Anaanaa and Naujánguit Members
of the Vaigat Formation (West Greenland Basalt Group)
and, although it is generally poorly exposed, it has been
recognised at many localities on Nuussuaq (Piasecki et
al. 1992), locally on the north coast of Disko, and locally
on Svartenhuk Halvø (Fig. 73; J.G. Larsen & Pulvertaft
2000). On the north coast of Nuussuaq, the formation
has been recognised both east and west of the Ikorfat fault.
It is present in the Tunorsuaq valley and has been locally
observed in the Itilli and Aaffarsuaq valleys (Floris 1972).
West of Ataa on the south coast of Nuussuaq, the formation
forms a thin unit dominated by marine mudstones
below the hyaloclastites of the Vaigat Formation. East of
Ataa, it is sandwiched between the sandstones of the
Quikavsak Formation and overlying non-marine mudstones
referred to the Naujât Member of the Atanikerluk
Formation (see also Koch 1959 pp. 78–79).
Type section. The outcrop section at Kangilia where the
Eqalulik Formation conformably overlies the Kangilia
Formation is very poorly exposed (Figs 74, 87, 118). A
complete, well-preserved section through the formation
was cored from 598 m to 496.5 m in the GANE#1 well
(Figs 65, 119) and this is therefore chosen as the type section
(Fig. 119). The cores are stored at GEUS in Copen -
hagen. The GANE#1 well is located at 70°28.25´N,
54°00.40´W.
Reference section. Reference sections occur on central
Nuussuaq in Agatdalen (Plate 3) and Aaffarsuaq (Fig
83), and on the south coast of Nuussuaq at Ippigaar suk -
kløften (Fig. 120).
In the GANK#1 well, a reference section was cored
from 333 m to 114.9 m (Fig. 121), and the formation
was also cored in the sidetrack well GANK#1A from
332.9 m to 218.6 m. The cores are stored at GEUS.
133

Eqalulik Formation
Kangilia Formation
Fig. 118. Exposure of the Eqalulik Formation overlying the Kangilia Formation at Kangilia. The photo shows the lower c. 20 m of the formation;
for location, see Fig. 74.
Thickness. On the north coast of Nuussuaq, the formation
ranges from 100 to 160 m thick, in Agatdalen it is
approximately 12 m thick (H.J. Hansen 1970), and in
Aaffarsuaq it is less than 20 m in thickness. In the
GANE#1A well, the formation is 102 m thick and it is
218 m thick in the GANK#1 well. The very variable
thickness of the formation is the result of varying proportions
of tuffaceous material (the presence of which
defines the formation) and intensive loading and deformation
of the mudstones by prograding thick lobes of
submarine basaltic breccia beds.
Lithology. The formation comprises mudstones, tuff beds
and volcaniclastic sandstones; the latter lithologies are
essential to the definition of the formation (Fig. 122).
Internal structures in the mudstones cannot be recognised
due to poor exposure. The thicker sandstone units consist
of amalgamated graded beds composed of fine- to
very coarse-grained, volcaniclastic sandstones with scattered
pebble-sized volcanic and mudstone clasts. Parallel
lamination, current cross-lamination and dish structures
have locally been observed within the graded beds. In some
areas volcanic material may constitute up to 25% of the
section (A.K. Pedersen 1978) and fossils are common
(Rosenkrantz 1970; Floris 1972). The tuff beds are up
to 7 m thick at Kangilia, and tuff beds up to several
metres thick are also seen in Danienkløft (Tunorsuaq)
and in Koralkløft (Ilugissoq; Figs 2, 74). Most of these
tuff beds contain scleractinian corals; these are without
preferred orientation, but only slightly worn (Floris
1972).
In the GANE#1 well the formation consists of mudstones,
interbedded quartz-rich, siliciclastic and volcaniclastic
sandstones and mudstones, muddy sandstones
and chaotic beds (Dam 1996b). Volcanic clasts and
rounded basement pebbles and angular mudstone ripup
clasts are common, and concretions and plant debris
are locally present (Fig. 119). Several thinning- and fining-upward
successions have been recognised in the core.
These are sharply based and consist of amalgamated normally
graded, very coarse- to coarse-grained sandstone
beds passing upwards into thinly interbedded sandstones
and mudstones. Occasionally the sandstone beds are
internally stratified, showing parallel-lamination or crosslamination,
dish structures and soft sediment folds.
Sandstones are occasionally burrowed and escape burrows
134

GANE#1
Vaigat Fm
Anaanaa Mb
m
Hyaloclastites
500
GANE#1A
Eqalulik Formation
550
m
550
600
600
First appearance of
hyaloclastite clasts
Agatdal Formation
640
vf
clay si
f m c vc
sand pb
650
Fig. 119. Type section of the Eqalulik
Formation in the GANE#1 and 1A wells
on western Nuussuaq. For location, see
Fig. 65; for legend, see Plate 1.
700
vf
clay si
f m c vc
sand
pb
135

Quikavsak Formation Eqalulik Fm Vaigat Formation
m
300
250
200
150
100
50
0
cl
si
sand
Boundaries. The lower boundary is placed at the base of
the first volcaniclastic sandstones or tuffs. This boundco
pb
Fig. 120. Reference section of the Eqalulik Formation overlying the
Paatuutkløften Member (Quikavsak Formation) at Ippigaarsukkløften
on southern Nuussuaq (for location, see Fig. 40). The upper part of
the Eqalulik Formation comprises fine-grained, tuffaceous mudstones
deposited at water depths up to 700 m, as demonstrated by
the height of the foresets in the overlying and laterally equivalent hyaloclastite
breccias. Modified from Dam & Nøhr-Hansen (2001). For
legend, see Plate 1.
are present in a few beds. Mudstone laminae show normal
grading. The chaotic beds in the GANE#1 well consist
of homogenised mudstones with evenly scattered
sand grains, granules, volcanic clasts and concretions.
The beds are interbedded with structureless muddy sandstones
and slumped mudstones showing contorted bedding
(Fig. 119; Dam 1996b).
Fossils. The formation has yielded a very rich fauna, particularly
in the Kangilia section where the concretions
in the mudstones include gastropods, bivalves, corals,
echinoderms and nautiloids, and also foraminifera,
crinoids and serpulids. The bivalve Thyasira (Conchocele)
aff. T. conradi (Rosenkrantz) and the pectinid Propeamussium
ignoratum Ravn are especially common in the
concretions together with a large thick-shelled Echinocorys,
Hercoglossa groenlandica (Rosenkrantz) and stems of
Isselicrinus groenlandicus Wienberg Rasmussen (Rosen -
krantz 1970; Henderson et al. 1976; Kollmann & Peel
1983; Petersen & Vedelsby 2000). A fish fauna is also
represented in the concretions (Bendix-Almgreen 1969)
and scleractinian corals and coccoliths have been reported
from the volcaniclastic sandstones (Floris 1972; Jürgensen
& Mikkelsen 1974). Some corals are attached to tuff
clasts, indicating that this was their original substrate. Their
random orientation suggests, however, that they are redeposited,
but as they are only slightly worn, transport distances
must have been short (Floris 1972). A sparse
nannoplankton and dinocyst flora is present at most
localities (Piasecki et al. 1992; Nøhr-Hansen et al. 2002),
including the mudstones at the base of the volcanic breccias
of the Vaigat Formation along the south coast of
Nuussuaq. The trace fossils Planolites isp. and Helminthopsis
horizontalis have been recognised in the GANE#1
and GANK#1 cores (Dam 1996b, c).
Depositional environment. The macrofossils and the
dinocysts indicate a marine depositional environment.
Based on the height of the overlying foresets in the hyaloclastite
breccias, the water depth can be estimated to
have been up to 700 m (A.K. Pedersen et al. 1993). The
sandstones are interpreted as the deposits of waning
stage high- to low-density turbidity currents. However,
tuff layers deposited from suspension have also been
recorded (A.K. Pedersen et al. 1989). Volcanism started
from eruption centres in the north-western and western
part of the region erupting directly into a deep marine
environment covering large parts of Nuussuaq and northern
Disko. The fossiliferous volcaniclastic sandstones
and tuffs represent the distal bottomsets of major hyaloclastite
beds of the Vaigat Formation (A.K. Pedersen
1985), the result of sediment gravity flows that transported
volcanic detritus and fossils into deeper water.
136

Fig. 121. Well reference section of the
Eqalulik Formation in the GANK#1 well.
For location, see Fig. 65; for legend, see
Plate 1.
m
250
Vaigat Fm
Annaanaa Mb
m
GANK#1
110 Hyaloclastites
Eqalulik Formation
300
150
?Kangilia Formation
Eqalulik Formation
350
200
400
clay si
vf
f m c vc
sand pb
250
vf
clay si
f m c vc
sand
pb
ary is, however, difficult to place in the field since outcrops
are generally very poor in these mudstone-domi -
nated successions. Along the north coast of Nuussuaq and
in the Tunorsuaq valley, a conspicuous change in the
colour of bottom sediment in small streams draining the
local lithologies has been observed to occur at a distinctive
level high in the sections. In the lower part of the
sections, the stream-bed sediments are ochreous whereas
this colouring is not present at higher levels; this change
may reflect the sulphide content in the mudstones of
the two formations and thus aid localisation of the formation
boundary. If so, the mudstones of the Kangilia
Formation were deposited in a poorly oxygenated, deepwater
environment in contrast to the Eqalulik Formation
where more oxygenated conditions could have resulted
from intermittent disturbance of bottom waters by progradation
of volcanic breccias.
The upper boundary is generally placed at the base of
the West Greenland Basalt Group, at the base of the
major hyaloclastic foreset beds of the Vaigat Formation
or at sills situated along the base of the Vaigat Formation
(Hald & Pedersen 1975; A.K. Pedersen et al. 1993). On
southern Nuussuaq, however, between Ataa and Ippigaar -
sukkløften (Fig. 40), the marine conditions prevailing during
deposition of the Eqalulik Formation were succeeded
by lacustrine environments, and consequently the Eqalulik
Formation is overlain by non-marine shales of the
Atanikerluk Formation (A.K. Pedersen et al. 1996; G.K.
Pedersen et al. 1998).
Geological age. The Eqalulik Formation is visibly diachronous,
reflecting the progressive eastward progradation
of the hyaloclastite fans which are very well exposed
along the slopes overlooking the south coast of Nuussuaq
137

of the Vaigat Formation in the north-western part of the
basin (Nøhr-Hansen et al. 2002). The tuffs of the
Abraham Member (see below) have a unique composition
with graphite and native iron that allows them to
be correlated with the volcanic Asuk Member (A.K.
Pedersen et al. 1989).
Subdivision. The volcaniclastic sediments in Agatdalen
and Qilakitsoq will continue to be assigned to a separate
member, the Abraham Member, because of their
unique geochemical composition which permits correlation
of the sediments with the volcanic Asuk Member
of the Vaigat Formation.
Abraham Member
revised member
History. The Abraham Member was established by Rosen -
krantz (in: Koch 1959 pp. 75–78) as the uppermost
member of the Agatdal Formation, but is now included
in the Eqalulik Formation on the basis of the characteristic
content of volcaniclastic material.
Fig. 122. Fossiliferous, volcaniclastic sandstones of the Eqalulik
Formation at Danienrygge. Pencil (encircled) and person for scale.
(A.K. Pedersen et al. 1993). However, the biostratigraphic
resolution is in most cases not good enough to resolve
this diachronism. The macrofauna at the type locality and
on central Nuussuaq indicates an Early Danian age
(Rosenkrantz 1970; Floris 1972; Henderson et al. 1976).
The coccolith assemblage has been related to the NP3
nannoplankton zone by Jürgensen & Mikkelsen (1974);
however, new dinocyst and nannoplankton data indicate
an NP4 – possibly base NP5 zone age (latest Danian
– early Selandian; Nøhr-Hansen et al. 2002). 40 Ar/ 39 Ar
age determinations of the volcanic rocks of the Anaanaa
Member (Vaigat Formation) overlying the Eqalulik For -
mation yield an age of 60.7 ± 1.0 (recalculated from
Storey et al. 1998).
Correlation. On the basis of dinocyst markers, the strata
in the type section can be correlated with the volcanic
hyaloclastites of the Anaanaa and Naujánguit Members
Name. After Abraham Løvstrøm from Niaqornat, who
for 30 years was a member of Rosenkrantz’s expeditions
to Nuussuaq (Fig. 7).
Distribution. The Abraham Member is known from two
localities in the northernmost part of the Agatdalen valley
(Fig. 113) and from the Qilakitsoq area in the
Aaffarsuaq valley (Fig. 82).
Type section. The type section of the Abraham Member
is in Turritellakløft at the northern end of Agatdalen
(Fig. 113, 114, Plate 3, section 1). The type section is
located at 70°35.01´N, 53°08.02´W.
Reference section. A reference section occurs in ‘Ravine 4’
east of Qilakitsoq (Figs 82, 83).
Thickness. The thickness of the Abraham Member is
approximately 12 m in the type section, 10 m in
Qaersutjægerdal in Agatdalen and 10–20 m at Qilakitsoq.
Lithology. The Abraham Member consists of black and
grey sandy mudstones intercalated with fossiliferous
reworked volcaniclastic sandstones and basement pebble
conglomerates (Figs 114, 115, Plate 3). Volcanic
material may constitute up to 25% of the section (A.K.
138

Pedersen 1978). The beds are usually structureless, but
cross-bedding has been recognised locally. Volcaniclastic
sandstones also occur as thin streaks in the mudstones
and may include spherules of volcanic glass or tuff with
a distinct chemical composition known only from the
Asuk Member erupted from the Ilugissoq graphite andesite
volcano (A.K. Pedersen 1985; A.K. Pedersen & Larsen
2006). In the lower part of the member, the mudstones
are very dark, fossiliferous and rich in concretions. At one
horizon, in situ corals are present in small bioherms,
10–20 cm high and less than 1 m wide (Plate 3, section
4). This horizon can be followed for more than a kilometre
on the eastern bank of Qaersutjægerdal. The content
of volcaniclastic sandstones increases upwards in
the section.
Fossils. A sparse but diverse marine fauna and flora has
been recorded from the Abraham Member, comprising
scleractinian corals, echinoids, bivalves, gastropods, crustaceans,
fish remains and palynomorphs (Bendix-
Almgreen 1969; Rosenkrantz 1970; Floris 1972; Koll -
mann & Peel 1983; Piasecki et al. 1992; Petersen &
Vedelsby 2000).
Depositional environment. The macrofossil content in the
lower part of the member indicates a marine depositional
environment. However, an increase up-section in
terrestrially derived palynomorphs indicates that the
environment became increasingly brackish with time.
Sedimentary structures in the volcaniclastic sandstones
indicate deposition from turbidity currents. The corals
suggest a shallow water (50?–80 m) marine environment
in a warm temperate climate (Floris 1972), but where
the corals were redeposited the water depth may well
have exceeded 80 m.
Boundaries. A sharp lithological boundary occurs between
the sandstones of the Agatdal Formation and the interbedded
mudstones and volcaniclastic sandstones of the
Abraham Member (Figs 114, 115). At Qilakitsoq and in
the northern part of Agatdalen, the Abraham Member
is succeeded by hyaloclastites of the Naujánguit Member,
whereas in the eastern part of Agatdalen the Abraham
Member is succeeded by hyaloclastites of the Tunoqqu
Member (A.K. Pedersen 1978; Piasecki et al. 1992; A.K.
Pedersen, personal communication 1999).
Geological age. As for the Eqalulik Formation, i.e. latest
Danian to early Selandian.
Correlation. The geochemical correlation of the Abraham
Member with the hyaloclastites of the Asuk Member of
the Vaigat Formation (A.K. Pedersen 1978, 1985; A.K.
Pedersen & Larsen 2006) ties these isolated outcrops to
the mapped volcanic succession on the south coast of
Nuussuaq (A.K. Pedersen et al. 1993).
Atanikerluk Formation
new formation
History. The Atanikerluk Formation comprises the synvolcanic
non-marine sediments in the Nuussuaq Basin;
in the eastern part of the basin, it includes almost all the
sediments overlying the Atane Formation (Fig. 16). It is
divided into five members (Fig. 123), which are correlated
to members in the volcanic Vaigat and Maligât
Formations (Fig. 131). The intra- and post-volcanic sediments
of the Nuussuaq Basin are not included in the
Nuussuaq Group and are therefore not discussed here.
Koch 1959
Nuussuaq
Nuussuaq
This paper
Disko
Fig. 123. Lithostratigraphical subdivisions
of the synvolcanic, non-marine deposits of
the Nuussuaq Basin.
Upper
Atanikerdluk
Formation
Point 976 Member
Aussivik Member
Umiussat Member Umiussat Member Umiussat Member
Naujât Member
Quikavsak Member
Assoq Member
Naujât Member
Quikavsak
Formation
Assoq Member
Pingu Member
Akunneq Member
Naujât Mb
Not present
Atanikerluk
Formation
139

Illukunnguaq
Ujarasussuk
Nuugaarsuk
Akunneq
Sullorsuaq
Vaigat
Q E Q E R T A R S U A Q
Inngigissoq
Pingu
D I S K O
69°45’
Sorte Hak
Storbræen
Frederik Lange Dal
Sullorsuaq Kvandalen
Aqajaruata
Qaqqaa
Aqajarua
Mudderbugten
Daugaard-Jensen Dal
Sermersuaq
Laksedalen
Killussaatsut Kuuat
Blåbærdalen K uk Qaamasoq
Akuliarutsip Qaqqaa
Skorstensfjeldet
Gule Ryg
Flakkerhuk
t
69°30’
Killussaatsut
Quaternary cover
Maligât Formation
Siniffik
Kuuk Qaamasoq
Tuapaat
Qaqqaat
Marraat Nuuk
Killuusat
Innanguit
Illunnguaq
Tuapaat
Aamaruutissat
Skansen
Innaarsuit
Skansen
Intrusion
Atanikerluk Formation
Sandstone
Atanikerluk Formation
Mudstone
Atane Formation
Skansen Member
Ice
Sea/lake
Assoq
Niuluut
53°
5 km
52°30’
500
Contour in metres
52°
Fig. 124. Geological map showing the distribution of the Atane and Atanikerluk Formations on eastern Disko, simplified from A.K. Pedersen
et al. (2001). Note that the outcrops of the Atanikerluk Formation are discontinuous. Contour interval is 200 m. For location, see Fig. 2.
140

In detail, however, the boundary between the Atanikerluk
Formation and the volcanic formations can be complex,
hyaloclastite breccias and invasive lavas interdigitating with
the sedimentary succession. These sediments, interstratified
locally with the lowermost volcanic layers, are
intimately associated with the uppermost Nuussuaq
Group strata and are thus referred to the Atanikerluk
Formation where demonstrably related to an interdigitating
volcanic–sediment facies front (Figs 17, 131).
Two new formations, the Quikavsak Formation and
the Atanikerluk Formation, replace the ‘Upper Atani kerd -
luk Formation’ of Nordenskiöld (1871), Troelsen (1956)
and Koch (1959). The term ‘Upper Atanikerdluk For -
mation’ dates back to Nordenskiöld (1871), who used
this name for the beds (Öfre Atanekerdluklagren) containing
the upper flora in the Atanikerluk area. The plant
fossils occur in concretions that are dark grey on fresh
surfaces but weather to a dark red colour (Nordenskiöld
1871 pp. 1051–52). Koch (1959) reported that these
concretions contain the Upper Atanikerdluk A flora of
Heer (1883a, b) and that they occur in his Quikavsak
Member, i.e. the Quikavsak Formation of the present
paper. The name Atanikerluk Formation is proposed
because it does not imply the existence of a ‘Lower
Atanikerd luk Formation’. Although a Lower Atanikerdluk
Flora was mentioned by Heer (1868), this originated
from the Atane Formation as recognised as early as 1871
by Nordenskiöld.
Koch (1959) subdivided the Upper Atanikerdluk
Formation into five members on Nuussuaq (Fig. 123)
but attempted no subdivision of the formation on Disko.
His Quikavsak Member is here established as the Qui -
kavsak Formation. Two of Koch’s members on Nuus -
suaq are retained (the Naujât and Umiussat Members),
whereas the Aussivik and Point 976 Members are abandoned
and the sediments are referred to the new Assoq
Member. The reason for this is that the Aussivik and
Point 976 Members are only found in a very small area
of south-eastern Nuussuaq (A.K. Pedersen et al. 2007b).
On Disko, a subdivision into five members is proposed
(the Naujât, Akunneq, Pingu, Umiussat, and Assoq Mem -
bers; Fig. 123). The subdivision of the Atanikerluk
Formation into five members reflects the dramatic palaeogeographic
changes that accompanied the intense volcanic
activity.
Name. The formation is named after the Atanikerluk
peninsula formed by a sill on the south coast of Nuussuaq
(Fig. 40). The name was formerly spelled Atanekerdluk
or Atanikerdluk.
Distribution. The Atanikerluk Formation is known on
south-east Nuussuaq (Saqqaqdalen, Atanikerluk, Kingit -
toq, Paatuut, and Ataata Kuua), on central Nuussuaq
(Nassaat and locally in Aaffarsuaq), on eastern Disko
(Assoq, Tuapaat Qaqqaat, Gule Ryg, Pingu, Nuugaarsuk,
Frederik Lange Dal) and central Disko (Daugaard Jensen
Dal and Sorte Hak; Figs 2, 40, 124). In the Atanikerluk
area, the formation was mapped in great detail by Koch
& Pedersen (1960). Paleocene siliciclastic sediments are
also present on Svartenhuk Halvø, where they are overlain
by the volcanic Vaigat and Svartenhuk Formations
(J.G. Larsen, personal communication 2008). These sediments
remain unstudied in detail and the distribution
of marine pre-volcanic, marine synvolcanic and nonmarine
synvolcanic deposits is not known at present. In
the future, Paleocene non-marine, synvolcanic sediments
on Svartenhuk Halvø may be established as one or more
members within the Atanikerluk Formation.
Type section. The section in the south-facing slope between
Atanikerluk and Tartunaq on south-east Nuussuaq is
retained as the type section (Figs 125, 126) for the
Atanikerluk Formation. This was described in detail by
Koch (1959), who defined type sections for several members
of the formation in this area. The type section is
located at 70° 03.63´N, 52°13.53´W.
Reference sections. Reference sections of the Atanikerluk
Formation are found at Kingittoq, at Pingu and in the
Tuapaat area (Figs 7, 132, 140). The stratigraphic succession
in north-east Disko has been compiled from the
(mainly sedimentary) sections on both sides of Akunneq
and the volcanic succession at Aqajaruata Qaqqaa, south
of Akunneq (A.K. Pedersen et al. 2005) (Figs 124, 131).
Thickness. The Atanikerluk Formation is up to 500 m
thick in a composite section, but individual outcrops
reach thicknesses of c. 400 m (Pingu), c. 300 m (Kingittoq,
Atanikerluk) and 200–250 m (Saqqaqdalen) (Figs 126,
128). At Tuapaat Qaqqaat, the thickness is difficult to
measure due to landslides and interbedding of sediments
and invasive lava flows (Fig. 140). Invasive lava flows are
discussed below under ‘Lithology’.
Lithology. The Atanikerluk Formation comprises mudstones,
heterolithic sandstones, and fine-grained, loosely
cemented sandstones. Mudstones are dominant in the
Naujât and Pingu Members (Fig. 127) and in the lower
part of the Assoq Member, whereas very friable sandstones
characterise the Akunneq and Umiussat Members
and the upper part of the Assoq Member. On a regional
141

Naujât Member
Qallorsuaq
‘Keglen’
Iviangernat
Assoq Member
invasive lava
Atanikerluk Formation
Umiussat Member
subaerial lava flow
Atane Formation
Kingittoq Member
Fig. 125. The coastal slope above Atanikerluk where Koch (1959) described the strata of the Atanikerluk Formation (for location, see Fig.
40). The peak at Iviangernat is 1031 m a.s.l. The Albian to Cenomanian Kingittoq Member of the Atane Formation is up to 500 m thick
and is overlain by the Paleocene Atanikerluk Formation (see Figs 16, 17).
scale, the formation comprises two coarsening-upward
successions that may include thinner, coarsening-upward
successions on a local scale (Figs 16, 131).
The mudstones are grey to dark grey, with abundant
silt-sized particles and with kaolinite and quartz as the
dominant minerals. In addition, gibbsite in subordinate
amounts has been detected consistently in samples from
the Pingu Member and commonly in the Assoq Member.
Locally, rows of small, yellowish brown siderite concretions
occur in the mudstones (G.K. Pedersen 1989; G.K.
Pedersen et al. 1998). Reworked Cretaceous palynomorphs
are found in the lowest part of the Atanikerluk Formation
at Akunneq (Hjortkjær 1991), suggesting that the formation
also contains redeposited silt and clay. Interbedded
with the mudstones are thin layers of tuff. The particles
are in the coarse sand fraction and have a brownish colour
that weathers to pale buff or white. The strong alteration
precludes a determination of the original chemical composition
of the volcanic glass.
The sandstones are weakly cemented, and in several
outcrops the lithology may be better described as sand.
Colours range from pale grey to deep yellow, and fine
coal debris is common. The sand or sandstones are generally
fine- to medium-grained; coarser grain sizes occur
but are volumetrically insignificant. Chert pebbles derived
from Ordovician sediments occur in the coarser facies,
as also seen locally in the Atane Formation. The sediments
of the Atanikerluk Formation could therefore include
material reworked from Cretaceous Atane Formation sand
or sandstones. This is supported by the occurrences of
few Paleocene palynomorphs together with more numerous
Cretaceous spores and pollen in the lower part of the
Akunneq Member at Pingu (Fig. 132, 285–355 m).
The siliciclastic sediments are interbedded with volcanic
rocks such as hyaloclastite breccias, invasive or subaqueous
lava flows and tuffs. Hyaloclastite breccias
comprise particles ranging from boulder-sized pillow
fragments to sand-sized grains of glass; these rocks formed
142

Fig. 126. Composite type section of the
Atanikerluk Formation from the
Atanikerluk area between Naajaat and
Umiusat, south-eastern Nuussuaq (for
location, see Fig. 40). 1: Section through
the Naujât Member from Saqqaqdalen at
the type locality defined by Koch (1959)
(Fig. 129). 2: Sections through the
Umiussat Member from discontinuous
outcrops in the Umiusat area (Figs 136,
137). 3: Section through the upper part of
the Naujât Member and the upper part of
the Assoq Member, formerly the Point 976
Member of Koch (1959) from discontinuous
outcrops below Keglen (Fig. 125). For
legend, see Plate 1.
Atanikerluk Formation
Naujât Member
m
180
170
160
150
140
130
120
110
100
90
80
70
60
50
40
30
20
10
Quikavsak
Formation
0
1 3
t 5
t 2,4,5
t 3,1,2
Atanikerluk Formation
Naujât Member Umiussat Member
Assoq Member
?
m
50
40
30
20
10
0
50
* *
40
30
20
10
0
30
20
10
0
20
10
0
2
vf
clay silt
f m c vc
sand
vf
clay silt
f m c vc
sand
when lava flowed into water. The breccias are often foreset-bedded
and the height of the foresets provides an
indication of water depth (Jones & Nelson 1970; A.K.
Pedersen et al. 1996; G.K. Pedersen et al. 1998). Invasive
or subaqueous lava flows formed from large volumes of
lava that reached the lake floor and continued into
(invaded) the unconsolidated sediment without forming
breccias (Schmincke 1967; Duffield et al. 1986; L.M.
Larsen & Pedersen 1990; Tucker & Scott 2009). Invasive
or subaqueous lava flows can be traced laterally into sub-
143

Naujât Member
Fig. 127. Reference locality of the Naujât
Member (Atanikerluk Formation) at
Kingittoq where lacustrine mudstones
overlie the Atane Formation (see also G.K.
Pedersen et al. 1998 fig. 7). For location,
see Fig. 2.
sill
Atane Formation
aerial lava flows and are thus different from sills, and are
only slightly younger than the sediments they invade.
Many of the invasive lava flows have retained their chemical
composition and may thus be correlated to the volcanic
lithostratigraphy. Layers of tuff are composed of
sand-sized particles, and typically are less than 3 cm
thick. The volcanic glass is strongly altered, and it is
rarely possible to determine the original chemical composition
of the glass.
Fossils. The Atanikerluk Formation contains a rich macro -
flora (Koch 1959, 1963, 1964), which Koch referred to
the Paleocene Macclintockia Zone characterised by Metasequoia
occidentalis, Cercidiphyllum arcticum, Macclin -
tockia Kanei, Macclintockia Lyalli and Dicotylophyllum
bellum (Koch 1959, 1963). Koch identified the Upper
Atanikerdluk A flora and the Upper Atanikerdluk B flora
of Heer (1883a, b) in the basal part of the formation (lowermost
Naujât Member). The Upper Atanikerdluk A
flora is also present in the Nuuk Qiterleq Member of the
Quikavsak Formation. The difference between the two
floras reflects changes in depositional environments, but
the floras are essentially coeval (Koch 1963). The diagnostic
species of the Macclintockia Zone occur in the
Naujât Member but have also been found in the Abraham
Member of the Eqalulik Formation (Koch 1963 p. 112).
The palynomorphs (mainly spores and pollen) of the
Atanikerluk Formation have been described by Croxton
(1978a, b), Hjortkjær (1991), L.M. Larsen et al. (1992),
Piasecki et al. (1992), Lanstorp (1999) and D.J. McIntyre,
personal communication 2009. Marine dinocysts and
rare bivalves have been reported locally from the Assoq
Member.
Depositional environment. The mudstones are interpreted
as lacustrine deposits on the basis of the high C/S ratios,
the absence of pyrite, the presence of terrestrial fossils
(macrofossil plants, spores and pollen) and the general
absence of marine dinocysts (Hjortkjær 1991; Piasecki
et al. 1992; G.K. Pedersen et al. 1998). The sandstones
are interpreted as dominantly fluvial and lacustrine in origin
on the basis of the current-generated sedimentary
structures, the lack of marine trace fossils, and their stratigraphic
position relative to the lacustrine mudstones.
Periodic marine inundations are indicated by the presence
of marine fossils in the mudstones of the Assoq
Member (Piasecki et al. 1992).
Boundaries. Over large areas, the Atanikerluk Formation
rests on an unconformity that defines the upper boundary
of the Atane Formation and which reflects a hiatus
of varying duration. In more restricted areas, the Atani -
kerluk Formation conformably overlies the Quikavsak
and Eqalulik Formations, or the volcanic Vaigat Formation
(Fig. 16). On south-eastern Nuussuaq, the Atanikerluk
Formation overlies either the Atane or the Quikavsak
Formation. Strata of the Atane Formation dip towards
the north-east, whereas the strata of the Atanikerluk
Formation are sub-horizontal (Fig. 129). Where the
Quikavsak Formation is present, its upper boundary is
also horizontal, indicating that the angular unconformity
between the Atane and Atanikerluk Formations
formed prior to the Danian. At other outcrops, the lacustrine
mudstones of the Naujât Member drape erosional
relief at the top of the Atane Formation (Figs 127, 130;
Pulvertaft 1989a; A.K. Pedersen et al. 2007a). The lower
boundary of the Atanikerluk Formation on Nuussuaq is
144

m
m
240
340 m
Pingu
Member
230
230
330
220
220
320
Atane Formation
Atanikerluk Formation
Skansen Member
Akunneq Member (lower part)
Akunneq Member (upper part)
210
200
190
180
170
160
150
140
130
120
110
100
90
80
70
60
50
40
30
20
Atanikerluk Formation
Atanikerluk Formation
Akunneq Member
Pingu Member Umiussat Member
210
200
190
180
170
160
150
140
130
120
110
100
90
80
70
60
50
40
30
20
t
t
t
t
t
t
t
t
t
6 8
50
30
15 4
15 6
25
36
30
10
5
concretion
Assoq Member
310
300
290
280
270
260
250
240
vf f m c vc
clay silt sand
Fig. 128. Type section of the Akunneq and
Pingu Members (Atanikerluk Formation)
measured at two closely spaced outcrops at
Pingu on eastern Disko (for outcrop, see
Fig. 132; for location, see Fig. 124). The
boundary between the lower and upper
parts of the Akunneq Member, at 110 m
on the log (left), is at 335 m a.s.l. (Fig
132). The locality is also the reference
section for the Atanikerluk Formation, the
Umiussat Member and the Assoq Member.
For legend, see Plate 1.
10
10
0
vf f m c vc f m c
clay silt sand pebbles
0
vf f m c vc f m c
clay silt sand pebbles
145

interpreted as a lacustrine flooding surface which can be
mapped westwards into the volcanic terrain where it separates
subaerial lavas of the Naujánguit Member from overlying
hyaloclastite breccias at or just above the base of
the Ordlingassoq Member (A.K. Pedersen 1985; A.K.
Pedersen et al. 1993; G.K. Pedersen et al. 1998) (Fig. 131).
On eastern Disko, the lowest member of the Atanikerluk
Formation is the dominantly fluvial Akunneq Member,
and the base of this member constitutes the lower boundary
of the formation; this is well exposed in the coastal
section from Pingu to Nuu gaarsuk (Figs 132, 133). The
upper boundary of the Atanikerluk Formation is either
a recent erosion surface or the boundary with volcanic
or volcaniclastic deposits of the Vaigat or Maligât
Formations (Figs 16, 131).
Geological age. The Atanikerluk Formation is dated by
dinocysts, pollen or plant macrofossils, and is constrained
by magnetostratigraphic and radiometric dating of the
correlative volcanic units. A maximum age for the
Atanikerluk Formation is obtained from the NP4 – possibly
early NP5 marine dinocysts in the underlying
Eqalulik Formation (Nøhr-Hansen et al. 2002). Samples
from the volcanic Ordlingassoq and Rinks Dal Members
give radiometric ages of 60.7–61.1 ± 0.5–1.0 Ma, recalculated
from Storey et al. (1998). This indicates an early
to mid-Paleocene (possibly Selandian) age for the
Atanikerluk Formation according to the timescale of
Gradstein et al. (2004) and Ogg et al. (2008).
Correlation. The two regional, coarsening-upward successions
recognised in the Atanikerluk Formation correlate
with the volcanic Ordlingassoq and Rinks Dal
Members of the Vaigat and Maligât Formations respectively
(Fig. 131). Correlation of individual members of
the Atanikerluk Formation to strata of the Vaigat For -
mation on Disko presents some difficulties due to lack
of exposures along the north coast of the island. The
Atanikerluk Formation is younger than the Eqalulik
Formation despite the similarity in macroplant fossils
between the Abraham and the Naujât Members.
Subdivision. The Atanikerluk Formation is subdivided into
five members: the Naujât, Akunneq, Pingu, Umiussat and
Assoq Members (Fig. 123).
Naujât Member
revised member
History. The Naujât Member was established by Koch
(1959). Its distribution is expanded here, but otherwise
the definition of the member is retained.
Name. The member is named from a small cove (modern
spelling Naajaat) on the south coast of Nuussuaq, just
west of Saqqaqdalen (Fig. 40; Koch 1955).
Distribution. The distribution of the Naujât Member
along the south-east coast of Nuussuaq was mapped by
Koch (1959 plates 5–7). He recognised the Naujât
Member in almost continuous outcrops and scree-covered
slopes on the western side of Saqqaqdalen and along
Naujât Member
U
S
70 m
S
Q
Atane
Formation
Fig. 129. Type locality of the Naujât
Member (Atanikerluk Formation) along
the western slope of Saqqaqdalen near
Naajaat (for location, see Fig. 40). An
angular unconformity is seen between the
Atane Formation and the Quikavsak
Formation (Q). The latter is conformably
overlain by lacustrine mudstones of the
Naujât Member, which is cut by a sill (S).
The outcrop of pale yellow sandstones in
the distance belongs to the Umiussat
Member (U).
146

Naujât Member
Atane Formation, Kingittoq Member
Fig. 130. Outcrop of the Naujât Member overlying the Atane Formation at Eqip Inaarsuata Qaqqaa, at the northern end of the Saqqaqdalen
valley (located as EIQ in Fig. 2). The lacustrine mudstones drape erosional relief on the top of the Atane Formation. The Naujât Member is
c. 200 m thick.
the coast from Naajaat to Kingittoq (Fig. 40). The member
was traced in scree and landslides in the Paatuut area,
and, at Ataata Kuua, in a thin succession between the mudstones
of the Eqalulik Formation and the hyaloclastite
breccias of the Ordlingassoq Member below Point 1010
m (Figs 15, 16; A.K. Pedersen et al. 1993, 2007b). In
Saqqaqdalen, the Naujât Member continues northwards
for about 25 km along the upper western slopes of the
valley (A.K. Pedersen et al. 2007a).
On Disko, the Naujât Member is known from scattered
outcrops along the north coast at Qorlortorsuaq
and towards Nuugaarsuk (G.K. Pedersen et al. 1998 fig.
12). The delineation of the member on Disko is also discussed
under the distribution of the Pingu Member.
Type section. The type section was described in the southwestern
end of Saqqaqdalen, above Naajaat, by Koch
(1959; Figs 124, 129). The type section is located at
70°04.10´N, 52°10.78´W.
Reference section. A reference section is proposed at
Kingittoq (Fig. 127). A sedimentological log is shown
in G.K. Pedersen et al. (1998 fig. 10).
Thickness. The Naujât Member is thickest on Nuussuaq,
up to 230 m at Kingittoq (Koch 1959) and in Saqqaqdalen
(G.K. Pedersen et al. 1998). On Disko, the member is
thin; up to 10 m are preserved at Qorlortorsuaq on the
north coast between Qullissat and Asuk (A.K. Pedersen
1985).
Lithology. The Naujât Member comprises dark grey to
black mudstones with thin, discontinuous layers of sandstones
and thin tuff beds. The tuffs are strongly altered
and the original chemical composition cannot be determined,
but examination of thin sections suggests that the
tuffs correlate with the Vaigat Formation. Mineralogically,
the mudstones are dominated by kaolinite and quartz with
minor feldspar, illite and smectite. Gibbsite has only
been identified in 15% of the samples, mostly from the
upper part of the member. Pyrite has not been detected.
147

Paatuut
1
Qullissat Giesecke M.
Inussuk Kingittoq
2 Fjeld
3
Atanikerluk
4
53°W
Vaigat Fm Maligât Fm
upper Rinks Dal
Mb
Akuarut unit
Skarvefjeld unit
lower Rinks Dal
Mb
Ordlingassoq
Mb
Naujánguit Mb
Subaerial
surface
Condensed
section
Condensed
section
Naujât Mb
Assoq
Mb
Umiussat
Mb
Naujât
Mb
Atanikerluk Formation
Hareøen
70°N
Nuussuaq
1
3
2 4
Disko
10
9
11
8
7
6
5 50 km
Anaanaa Mb
Eqalulik Fm
Skarvefjeld
5
Assoq
Marraat
6
Tuapaat
7
Peak
1123 m
8
Fr. Langes
Dal
9
Ingigissoq
10
Pingu
11
Vaigat Fm Maligât Fm
upper Rinks Dal
Mb
Akuarut unit
Skarvefjeld unit
lower Rinks Dal
Mb
Ordlingassoq
Mb
60.7±0.4
60.9±0.4
61.1±0.5
60.7±1.0
Naujánguit Mb 60.8±0.5
Assoq
Mb
Assoq Mb
Umiussat Mb
Pingu Mb
Akunneq Mb
Atanikerluk Formation
Anaanaa Mb
Subaerial lava flow
Subaqueous lava flow
Hyaloclastite breccia
Entablature zone
Columnar jointing
Sandstone
Lacustrine mudstone
Marine mudstone
Conglomerate
Coal
Marine dinoflagellate
Fig. 131. Simplified stratigraphic sections showing the relationships between the volcanic rocks (colour coded) of the Vaigat and Maligât
Formations (West Greenland Basalt Group) and the Atanikerluk Formation. The upper boundary of the Assoq Member is indicated (dashed
line). The invasive, subaqueous lavas are all assigned to the Maligât Formation. The radiometric ages are recalculated from Storey et al. (1998).
148

The TOC [Total Organic Carbon] content is high (up
to 11%) and C/S ratios are high (G.K. Pedersen et al.
1998). Perregaard & Schiener (1979) noted that the
organic matter is immature, consisting of exinite (c.
50%), vitrinite (c. 35%) and inertinite (c. 15%), and
that it is chemically dominated by saturated and aromatic
hydrocarbons. A study of palynofacies indicates a
predominance of brown and black lignite (Hjortkjær
1991).
Fossils. The Naujât Member has yielded well-preserved
macroplant fossils, the Upper Atanikerdluk flora A and
B of Heer (1883a, b; Koch 1959, 1963). Leaves from
deciduous trees are an important constituent in the flora
which includes: Cladophlebis groenlandica, Metasequoia
occidentalis, Cercidiphyllum arcticum, Dicotylophyllum
bellum, Dicotylophyllum Steenstrupianum, Macclintokia
Kanei, Macclintockia Lyalli and Credneria spectabilis (Koch
1963).
The assemblage of spores and pollen in the Naujât
Member was studied by Hjortkjær (1991). The flora is
dominated by palynomorphs of terrestrial origin, whereas
remains of lacustrine plants and algae are rare. Pollen of
Taxodium spp. are abundant. The stratigraphically important
mid-Paleocene species Momipites actinus and Caryapollenites
wodehouseia are present in this member.
Depositional environment. The Naujât Member is interpreted
as a succession of lacustrine mudstones (Koch
1959; Schiener & Leythaeuser, 1978; G.K. Pedersen et
al. 1998). The lake formed through damming by the
volcanic rocks of the Ordlingassoq Member, and it was
filled simultaneously by hyaloclastite breccias from the
west and siliciclastic mud from the east and south-east
(G.K. Pedersen et al. 1998). The abundance of kaolinite
among the clay minerals suggests that these have the
same provenance as the mudstones of the Cretaceous
Atane Formation, probably areas of deeply weathered
crystalline rocks east of the basin boundary fault.
Boundaries. The lower boundary of the Naujât Member
corresponds to the lower boundary of the Atanikerluk
Formation in the area where the Naujât Member occurs
(Figs 126, 129, 130). Mapping of the lower boundary
is difficult in the Paatuut and Ataata Kuua areas where
the member overlies marine mudstones of the Eqalulik
Formation. In this area, the Naujât Member is also
interbedded with the toesets of hyaloclastite breccias of
the Ordlingassoq Member (Fig. 17, locality 5). The upper
boundary of the Naujât Member is everywhere towards
either the Umiussat Member or the Ordlingassoq Member
of the Vaigat Formation (Fig. 136).
Geological age. Within the resolution of the dating methods,
the age of the Naujât Member lies within the age
range of the Atanikerluk Formation (i.e. early to mid-
Paleocene, see p. 146).
Correlation. The Naujât Member is coeval with the volcanic
breccias of the Ordlingassoq Member; both members
overlie the same lacustrine flooding surface (A.K.
Pedersen et al. 1993; G.K. Pedersen et al. 1998). The lacustrine
Naujât Member on Nuussuaq correlates with the
fluvial Akunneq Member on north-eastern Disko. The
palynomorph assemblages of the Naujât, Akunneq and
Pingu Members are similar, and the upper part of the
Naujât Member correlates with the Pingu Member (Figs
123, 131).
Akunneq Member
new member
History. The sediments now referred to the Akunneq
Member were formerly referred to the Upper Atanikerdluk
Formation (Koch 1964; Croxton 1978a section C2).
Name. The member is named after the Akunneq valley
between the Pingu and Inngigissoq mountains on the
north-east coast of Disko.
Distribution. The Akunneq Member is known from the
north-east coast of Disko (Pingu to Nuugaarsuk) and
southwards to Gule Ryg (Fig. 124).
Type section. The section at Pingu on the eastern side of
Akunneq is chosen as the type section (Figs 128, 132).
The type section is located at 69°47.53´N, 52°05.43´W.
Reference section. The section on the western side of
Akunneq is chosen as the reference section.
Thickness. The Akunneq Member is c.165 m thick at
Pingu but only c.145 m at Nuugaarsuk. Thus the member
decreases in thickness towards the west (Fig. 133).
Lithology. The Akunneq Member is dominated by very
friable sandstone. It comprises a coarse-grained lower
part and a finer-grained upper part, separated by a mudstone
horizon at 335 m a.s.l. in the Pingu–Akunneq sec-
149

Pingu 845 m
Upper Rinks Dal Member
sill
Umiussat
Member
Pingu
Member
Assoq Member
sill
sill
Inngigissoq
845 m
U. Rinks Dal Member
sill
P
Akunneq
Member
335 m a.s.l.
d
Akunneq Member
285 m a.s.l.
d
Atane Formation
Skansen Member
Fig. 132. Outcrop of Atanikerluk Formation in the area between Pingu and Inngigissoq on eastern Disko cut by several dykes (d) and sills
(for location, see Fig. 124). The boundary between the Atane Formation (Skansen Member) and the Atanikerluk Formation is set at 285 m
a.s.l. The boundary at 335 m a.s.l. separates the lower and upper parts of the Akunneq Member (for section, see Fig. 128). P, Pingu Member.
tion (Figs 132, 133). The lower part consists of large-scale
cross-beddded, coarse-grained sandstones that differ little
from the fluvial sandstones of the Atane Formation
(Figs 128, 134). The upper part is dominated by finegrained
white sands interbedded with thinner horizons
of mudstone, carbonaceous mudstone or thin coal seams.
Bedding planes in the sandstone are often draped by
coaly plant debris. Photogrammetric work shows that
the c. 5 m thick mudstones are laterally continuous over
a distance of 10 km, and that the proportion of finegrained
facies increases in a westerly direction from Pingu
to Nuugaarsuk. Locally, the upper sandstones include
2–3 m thick beds with low-angle, composite cross-bedding.
Bedform migration directions suggest westerly
palaeocurrents.
Fossils. Thin mudstone horizons in the Akunneq Member
contain Paleocene spores and pollen as well as reworked
species of Cretaceous (Cenomanian) age (Croxton 1978a,
b; Hjortkjær 1991, D.J. McIntyre, personal communication
2009). The upper part of the Akunneq Member
is dominated by Paleocene species identical to those
occurring in the Naujât and Pingu Members (Hjortkjær
1991; B.F. Hjortkjær, personal communication 1999).
The lower part of the Akunneq Member is dominated
by reworked Cenomanian species, and unquestionable
Paleocene species are scarce (B.F. Hjortkjær, personal
communication 1999; D.J. McIntyre, personal communication
2009).
Depositional environment. The Akunneq Member is interpreted
as a succession of sandy fluvial deposits interbedded
with thin lacustrine mudstones. The sandstones in
the lower part of the Akunneq Member are interpreted
as deposited in braided channels. The change in grainsize
and the ubiquitous coaly plant debris indicate lower
energy, and the occasional occurrence of sandy point bar
deposits suggests deposition in meandering fluvial channels.
The thin but laterally widespread mudstones are
interpreted as reflecting short-lived phases of lake formation,
and the coal beds represent peat formation.
Towards the west, in a downstream direction, the Akunneq
150

Fig. 133. Correlation of the members
within the Atanikerluk Formation on
north-east Disko. Note the general
thinning of units westwards from Pingu to
Nuugaarsuk. Altitudes above sea level are
indicated. For location, see Fig. 124; for
legend, see Plate 1.
m
700
Pingu
Assoq Member
600
Umiussat Member
m
600
Nuugaarsuk
500
400
300
220
Atane Formation Atanikerluk Formation
Skansen Member
Akunneq Member
Pingu Member
?
500
420
400
300
260
?
mud sand
mud sand
151

Fig. 134. The illustrated, coarse-grained,
fluvial sandstone unit, c. 30 m thick,
showing large-scale cross-bedding is
characteristic of the lower part of the
Akunneq Member on the western side
of Akunneq. The sandstone is abruptly
overlain by grey muddy sandstones, also
referred to the Akunneq Member. For
location, see Fig. 124.
Member becomes thinner with an increasing amount of
mudstone, which suggests that it was deposited on a
floodplain adjacent to the ‘Naujât lake’.
Boundaries. The lower boundary of the Akunneq Member
corresponds to the lower boundary of the Atanikerluk
Formation in the area of distribution of the Akunneq
Member (Fig. 132). The geological map of the Pingu area
shows that both the Atane and the Atanikerluk Formations
are subhorizontal in north-east Disko (A.K. Pedersen et
al. 2001). The boundary between the fluvial Skansen
Member and the fluvial Akunneq Member may be difficult
to identify in outcrops. In the Pingu area, the lower
boundary of the Akunneq Member is placed at the base
of a c. 3 m thick unit of bluish grey, laterally continuous
mudstones, which forms a terrace with a steep front.
The upper boundary of the Akunneq Member is placed
at the base of the mudstones of the Pingu Member (Figs
132, 133, 135).
Geological age. Reworked Cretaceous spores and pollen
dominate the lower part of the Akunneq Member, but
the few Paleocene forms show that the age of the Akunneq
Member lies within the age range of the Atanikerluk
Formation (i.e. early to mid-Paleocene, see above).
Correlation. The Akunneq Member is interpreted to correlate
with the lower or middle part of the Naujât Member.
Abundant landslides on the north coast of Disko obscure
the relationships between the Akunneq Member and the
Ordlingassoq Member of the Vaigat Formation (A.K.
Pedersen et al. 2005).
Pingu Member
new member
History. Sediments referred to the Pingu Member were
earlier described by Croxton (1978a section C2). Their
sedimentary facies and depositional environment were
discussed by G.K. Pedersen (1987, 1989). The deposits
were tentatively referred to the Naujât Member by G.K.
Pedersen (1987). The difference in mineralogy, the lack
of positive evidence that the Pingu and Naujât Members
are continuous, and the prominence of this mudstone
unit on north-east Disko are the reasons for erecting the
Pingu Member.
Name. The member is named from the mountain of
Pingu on north-east Disko (Figs 124, 132).
Distribution. The Pingu Member is only known from outcrops
on Disko. It is continuously exposed in the coastal
section from Pingu to Nuugaarsuk and can be traced
south-west of Pingu to Gule Ryg (Fig. 124).
Type section. The section on the north side of Pingu (east
of Akunneq) is chosen as the type section of the Pingu
Member (Figs 128, 135). The type section is located at
69°47.13´N, 52°02.12´W.
Reference section. The section between Akunneq and Nuu -
gaarsuk is chosen as the reference section of the Pingu
Member (Figs 124, 133).
152

Fig. 135. Type locality of the Pingu
Member on the north side of Pingu (for
location, see Fig. 124). Note the sharp
lower boundary with the Akunneq
Member and the transitional upper
boundary with the Umiussat Member.
Umiussat Member
25 m
Pingu Member
Akunneq
Member
Thickness. The Pingu Member is 85 m thick at Pingu,
probably thinning towards Nuugaarsuk, although the
thickness is difficult to measure at the latter locality due
to landslides (Fig. 133). The member is more than 30
m thick at Gule Ryg.
Lithology. The Pingu Member consists of dark grey mudstones
interbedded with thin layers of tuff and finegrained
sandstone beds that increase in frequency upwards.
The member thus constitutes an overall coarseningupward
succession (Fig. 128; G.K. Pedersen 1989).
Mineralogically, the mudstones consist of kaolinite
and quartz with a little illite and feldspar; neither calcite
nor pyrite has been detected. Gibbsite is found in 96%
of the samples where it makes up 5–10% of the sediment.
Siderite occurs in small concretions that weather bright
yellow. The mudstones are rich in organic matter (up to
8%), most of which is terrestrial (G.K. Pedersen 1989).
A palynofacies study demonstrated the predominance
of brown and black wood (Hjortkjær 1991). The sandstones
are fine-grained, well-sorted and form thin beds
showing parallel lamination or current ripple cross-lamination.
Fossils. The assemblage of spores and pollen in the Pingu
Member was studied by Hjortkjær (1991), who found
that it corresponds to that of the Naujât Member. The
flora is dominated by palynomorphs of terrestrial origin,
whereas remains of lacustrine plants and algae are rare.
Pollen of Taxodium spp. are abundant. The stratigraphically
important mid-Paleocene species Momipites actinus
and Caryapollenites wodehouseia occur together with
a few specimens of the mid- to late Paleocene Insulapollenites
rugulatus (Hjortkjær 1991). Neither Croxton (1978a,
b) nor Hjortkjær (1991) observed marine dinocysts in
samples from the Pingu Member.
Depositional environment. The Pingu Member represents
a predominantly low energy depositional environment
characterised by settling of mud from suspension and occasional
deposition of sand from low energy sediment gravity
flows. The lack of marine fossils coupled with the
absence of both pyrite and its weathering product jarosite
indicates a lacustrine depositional environment. The
increasing number of sand layers up-section are interpreted
to record gradual progradation of the shoreline and consequent
filling of the lake (G.K. Pedersen 1989). The supply
of gibbsite to the lacustrine mud suggests input from
a new provenance area. The expanding areas of subaerial
basalt flows may have weathered to lateritic soils that
could have supplied gibbsite during deposition in the
‘Pingu lake’. This new provenance area is also reflected
in the mineralogy of the top of the lacustrine Naujât
Member.
Boundaries. The Pingu Member has a sharp lower and a
gradational upper boundary (Figs 128, 132, 135). The
lower boundary separates the lacustrine mudstones of
the Pingu Member from the underlying sandy fluvial
Akunneq Member; this abrupt boundary is overlain
either directly by mudstones or by a thin succession of
mudstones interbedded with sandstone layers and it is
interpreted as an erosional surface formed during lacustrine
drowning (Figs 128, 135). The upper boundary is
defined by the base of the Umiussat Member (Figs 128,
132, 133, 134, 135).
153

Geological age. The age of the Pingu Member is the same
that of the Atanikerluk Formation (i.e. early to mid-
Paleocene, see p. 146).
Correlation. The deposits assigned here to the Pingu
Member have been correlated with the Naujât Member
(Henderson et al. 1981 fig. 4). The assemblages of spores
and pollen in the two members are similar (Hjortkjær
1991), but the mineralogy differs, especially with respect
to the distribution of gibbsite. We interpret the Pingu
Member on Disko as correlating with the upper part of
the Naujât Member on Nuussuaq.
A correlation between the Pingu Member and the volcanic
Ordlingassoq Member cannot be proven because
the north coast of Disko is ravaged by landslides and
rock glaciers between Nuugaarsuk and Qullissat (A.K.
Pedersen et al. 2005). Between Pingu and Nuugaarsuk,
the oldest magmatic rocks have a composition corresponding
to the Maligât Formation (Fig. 131).
Umiussat Member
revised member
History. The Umiussat Member was established by Koch
(1959) on south-east Nuussuaq where it overlies the
Naujât Member. In the present paper the definition of
the Umiussat Member is retained, but its geographical
distribution is expanded.
Name. The member is named from the Umiusat ridge
on south-eastern Nuussuaq (Fig. 40).
Distribution. The Umiussat Member is known on southeast
Nuussuaq in the area between Naajaat and Kingittoq,
and in Saqqaqdalen. It covers a smaller area than the
Naujât Member. The Umiussat Member is also present
on eastern Disko between Nuugaarsuk and Pingu, and
at Gule Ryg (Figs 40, 124).
Type section. The type section of the Umiussat Member
of Koch (1959) at Umiusat is retained (Figs 126, 136).
The type section is located at 70°09.00´N, 52°26.57´W.
Reference section. The section on the north side of Pingu,
east of Akunneq, is suggested as a reference section for
the Umiussat Member (Figs 128, 132).
Thickness. The Umiussat Member is 70−100 m thick. It
is rarely well exposed, hence lateral variations in thickness
are not documented. The member is c. 80 m thick
at Pingu (Fig. 128) and c. 100 m thick in the Atanikerluk
area (Koch 1959).
Lithology. The Umiussat Member is dominated by fineto
medium-grained sands or sandstones which range in
colour from white or pale grey on Disko to yellow on
Nuussuaq. Comminuted plant debris is abundant and
outlines bedding planes and sedimentary structures such
as cross-lamination and cross-bedding. The sands or
sandstones are interbedded with 1–5 m thick mudstones,
Maligât Formation lava flows
35 m
Umiussat Member
Naujât Member
Fig. 136. Type locality of the Umiussat
Member (Atanikerluk Formation) at
Umiusat, south-eastern Nuussuaq (for
location, see Fig. 40). At the top of the
Naujât Member, an increase in the number
of thin sandstone beds results in a
transitional boundary between the two
members.
154

Fig. 137. Lower, sharp boundary of the
Assoq Member with the Umiussat Member
at Umiusat. See section 2 in the composite
sedimentological log in Fig. 126.
Maligât Formation
15 m
Assoq
Member
Umiussat Member
some of which include thin coal beds (Figs 126, 128, 137).
A 120 cm thick coal bed forms the top of the Umiussat
Member on north-east Disko (Fig. 131).
Fossils. No fossils have been reported from the Umiussat
Member.
Depositional environment. The sediments of the Umiussat
Member are interpreted to have been deposited in predominantly
braided fluvial channels and on floodplains.
Boundaries. The lower boundary with the Naujât Member
is transitional and is rarely well exposed (Fig. 136; Koch
1959). The lower boundary with the Pingu Member is
placed at an erosional surface separating the heterolithic
sandy mudstones at the top of the Pingu Member from
the overlying fluvial sandstones of the Umiussat Member
(Figs 128, 135). The upper boundary of the Umiussat
Member is placed at the drowning surface which forms
the lower boundary of the Assoq Member (Figs 133, 137).
Geological age. The age of the member lies within the age
range of the Atanikerluk Formation (i.e. early to mid-
Paleocene, see p. 146).
Correlation. The Umiussat Member is interpreted as
coeval with the uppermost subaerial lava flows of the
Ordlingassoq Member, and deposition of the Umiussat
Member probably continued during the break in volcanic
activity between the Vaigat and the Maligât Formations
(Fig. 131).
Assoq Member
new member
History. The sediments referred to the Assoq Member
include those overlying the Umiussat Member on Disko
as well as those referred to the Aussivik Member and the
Point 976 Member of Koch (1959) (Fig. 123). The
Aussivik and Point 976 Members are abandoned because
they are poorly exposed and only cover small areas on
south-eastern Nuussuaq.
Name. The member is named from the coastal mountain
slope at Assoq on southern Disko (Fig. 124).
Distribution. The geological map sheets 1:100 000 Uiffaq
and 1:100 000 Pingu show that the Assoq Member covers
most of Disko, east of the Disko Gneiss Ridge (A.K.
Pedersen et al. 2000, 2001). The area in which the Assoq
Member is distributed is strongly affected by landslides
and reliable outcrops are discontinuous (Fig. 124). On
Nuussuaq, the Assoq Member is present at Kingittoq,
between Umiusat and Saqqaqdalen, in the Atanikerluk
area and probably also on central Nuussuaq, east of the
Ikorfat fault (Fig. 40; A.K. Pedersen et al. 1993, 2002,
2007b).
Type section. The type section is at Assoq within a huge
landslipped block (Fig. 138). This locality has the best
exposures of the fissile mudstones, but neither the lower
nor the upper boundary of the Assoq Member is confi-
155

Lower Rinks Dal Member
subaqueous lava
Upper Rinks Dal Member
subaqueous lava
subaqueous lava
Assoq Member
invasive lava
55 m a.s.l.
invasive lava
Assoq Member
invasive lava
Fig. 138. Type locality of the Assoq Member at Assoq on the south coast of Disko (for location, see Fig. 124). The brownish black mudstones
of the Assoq Member are interbedded with invasive lava flows and overlain by subaqueous lava flows of the lower Rinks Dal Member of the
Maligât Formation (see Fig. 131). Sediments and interbedded volcanic rocks are part of a huge landslide, two blocks of which are separated
by the dash–dot line. The Assoq Member is also found at higher altitudes away from the coast (A.K. Pedersen et al. 2003). For log, see Fig.
139.
dently identified (Fig. 139). The type section is located
at 69°19.23´N, 53°09.10´W.
Reference sections. Reference sections are exposed on southern
Disko east of Assoq (Fig. 139), on northern Disko
at Pingu (Figs 124, 128), and on southern Nuussuaq at
Qallorsuaq (Keglen). The sediments here were formerly
referred to the Aussivik and Point 976 Members of Koch
(1959) (Figs 40, 125).
Thickness. The Assoq Member is up to c. 200 m thick,
but the thickness is difficult to measure in areas where
the sediments are interbedded with volcanic or intrusive
rocks and are subject to landslides.
Lithology. The Assoq Member constitutes a major, coarsening-upward
succession with a lower part dominated
by brownish black fissile mudstones, and an upper part
that is dominated by sands but also includes a single, 3
m thick, coal seam (Figs 126, 128, 138, 140). The mudstones
have TOC contents of up to 7%. The dominant
clay mineral is kaolinite, but gibbsite is also present in
most samples. Thin beds are cemented by siderite. Nume -
rous thin tuff layers are interbedded with the mudstones.
They are typically a few millimetres to a few centimetres
thick, deposited by settling through the water column.
Examination of thin sections shows that the tuff
is strongly altered diagenetically. The mudstones are
interbedded with hyaloclastite breccias and subaqueous
lava flows which formed where lava flows of the lower
Rinks Dal Member entered the ‘Assoq lake’ (L.M. Larsen
et al. 2006). Based on their chemical composition, the
invasive lava flows are correlated with various units within
the volcanic lower Rinks Dal Member (Figs 131, 139,
140).
156

m
130
125
110
t
t
invasive lava
lower Rinks Dal Mb
The upper part of the Assoq Member is dominated
by sands, often with comminuted plant debris. In the
scree-covered slopes at Tuapaat Qaqqaat and Qallorsuaq
(Keglen), the sands are yellow and fine-grained, but rarely
well exposed. At Pingu and Gule Ryg, the sedimentary
structures suggest deposition from traction currents in
a low-energy environment (Fig. 128). A thick coal bed
has been observed at the top of the Assoq Member (Fig.
141) which probably correlates to coal beds interbedded
with volcanic rocks at several localities west of Gule Ryg,
eastern Disko (L.M. Larsen & Pedersen 1990; A.K.
Pedersen et al. 2001) (Fig. 131). These sediments are
considered part of the Atanikerluk Formation as they
can be traced from continuous sedimentary successions
into the basal part of the subaerial lava flow succession.
The chemistry of these volcanic rocks corresponds to
the lower part of the upper Rinks Dal Member.
?Atane Formation Atanikerluk Formation
Assoq Member
105
40
35
30
25
10
5
0
t
s
t
s
s
t
t
t
t
t
t
sill
clay si sand
invasive lava
lower Rinks Dal Mb
8
10
10
10
20
30
12
10
22
30
10
20
3
7
10
10
invasive lava
lower Rinks Dal Mb
10
5
Fossils. Plant macrofossils are unevenly distributed in the
Assoq Member, but they are generally scarce. From the
Atanikerluk area, Koch (1959) reported a leaf of
Cercidiphyllum arcticum from the lower part (his Aussivik
Member) and pieces of fossil wood of Taxodioxylon type
from his Point 976 member. Bedding planes covered by
plant remains were observed west of Kingittoq by the present
authors. The freshwater bivalve Unio sp. occurs in
the upper, sandy part of the Assoq Member (Koch 1959).
Fish scales and bones are preserved in a concretion from
Akuliarusinnguaq (c. 4 km north of Gieseckes Monument;
Fig. 2).
The spores and pollen in the Assoq Member were
described by Hjortkjær (1991) and differ little from those
in the older members of the Atanikerluk Formation.
Piasecki et al. (1992) reported finds of marine dinocysts
in a few samples from the Assoq Member in southern
and eastern Disko. In the inner part of Kvandalen (Fig.
124), the mudstones are found to contain rare bivalves
(protobranchs?) and rare dinocysts (Piasecki et al. 1992).
A few marine dinocysts were found at Tuapaat Qaqqaat
at the top of the Assoq Member just below the basalt conglomerate
(Fig. 140).
Fig. 139. Type section of the Assoq Member at Assoq on the south
coast of Disko (for location, see Fig. 124). The lacustrine mudstones
contain numerous millimetre-thick tuff beds. For legend, see Plate 1.
157

Atanikerluk Formation
Assoq Member
m
510
500
450
400
380
280
250
200
150
100
invasive lava flows correlate to the lower Rinks Dal Member invasive lava flows correlate to the Akuarut unit
of the lower Rinks Dal Member
Depositional environment. At Skarvefjeld (Fig. 2), the
lower, shaly part of the Assoq Member is interbedded with
hyaloclastite breccias that are traced laterally into the
lower Rinks Dal Member (Heinesen 1987; L.M. Larsen
& Pedersen 1990). Water depths of 80−100 m are calculated
from the height of the foresets of the hyaloclastite
breccias. Similar interbedding of Assoq Member mudstones
and hyaloclastite breccias is also known from Sorte
Hak on central Disko, slightly east of the Disko Gneiss
Ridge (Fig. 124). The Assoq Member is interpreted as
lacustrine in origin, deposited within the ‘Assoq lake’. At
present it is not possible to demonstrate whether this
was one huge lake or several smaller lakes. Scarce marine
dinocysts indicate that the Assoq lake was subject to
marine inundations. The dinocysts were found in samples
from eastern and south-eastern Disko, but were not
recorded from Nuussuaq. This distribution, coupled
with a south-eastward tilting of an originally nearly horizontal
magmatic boundary (L.M. Larsen & Pedersen
1992) suggests that the marine inundations were from
the south. The upward transition from mudstones to
sandstones reflects shallowing and gradual fill of the
lake. During a break in clastic sediment input, peat accumulated
in a large swamp in eastern Disko, and resulted
in a thick coal bed (Fig. 141).
Boundaries. The lower boundary of the Assoq Member
is placed at the base of the mudstone succession, and is
interpreted as a lacustrine drowning surface (Figs 128,
137). On north-east Disko, the lower boundary overlies
a coal bed. The upper boundary is placed where the sediments
are overlain by subaerial lava flows of the Rinks
Dal Member. Note that locally thin tongues of sediment
within the lower Rinks Dal Member are assigned to the
Assoq Member; such sediment wedges are bounded
abruptly beneath and above by volcanic strata. At Tuapaat
Qaqqaat, the uppermost bed in the Assoq Member is a
conglomerate with clasts of basaltic rocks derived from
lava flows of the Akuarut unit of the Rinks Dal Member
(Fig. 140; L.M. Larsen & Pedersen 1990, 2009).
Atane Formation
Skansen Member
50
0
Covered by
scree
vf f m c vc f m c
clay silt sand pebbles
Fig. 140. Composite reference section of the Assoq Member at Tuapaat
Qaqqaat, south-eastern Disko (for location, see Fig. 124). Note the
occurrence of marine dinocysts at the top of the lacustrine section,
indicating a brief marine inundation. Colour coding of volcanic rocks
follows Fig. 131. For legend, see Plate 1.
158

Fig. 141. Upper part of the Assoq Member
including a 5.1 m thick coal bed. South
side of Blåbærdalen, eastern Disko (for
location, see Fig. 124). Correlative coal
beds are seen at several widely spaced
outcrops indicating the development of
large swamps. The sediments are overlain
by subaerial lava flows of the volcanic
Rinks Dal Member (see Fig. 131).
upper Rinks Dal Member
coal
Assoq Member
Geological age. The age of the Assoq Member lies within
the age range of the Atanikerluk Formation (i.e. early to
mid-Paleocene, see p. 146).
Correlation. On southern Disko, the lower, shaly, part of
the Assoq Member is interbedded with subaqueous lava
flows and hyaloclastite breccias, which continue westwards
into the Skarvefjeld unit (formerly Pahoehoe unit) of
the lower Rinks Dal Member (Fig. 131; Heinesen 1987;
L.M. Larsen & Pedersen 1990, 2009; A.K. Pedersen et
al. 2003; L.M. Larsen et al. 2006). On north-eastern
Disko (Akunneq and Pingu), the earliest volcanic rocks
are thick invasive lava flows with columnar jointing,
which invaded the uppermost part of the Umiussat
Member and the Assoq Member. The composition of
these volcanic rocks tie them to the uppermost lower
Rinks Dal Member and the Akuarut unit (formerly FeTi
unit) (Fig. 131; A.K. Pedersen et al. 2005; L.M. Larsen
et al. 2006; L.M. Larsen & Pedersen 2009).
On Nuussuaq, lava flows of the Akuarut unit invaded
mudstones of the Assoq Member and increased markedly
in thickness due to ponding of the lavas in the ‘Assoq lake’.
Throughout eastern Disko and southern Nuussuaq the
Assoq Member is thus interbedded with invasive flows
of the Rinks Dal Member, and the various volcanic facies
(breccias, invasive lavas or ponded subaerial lava flows)
are thought to reflect different extrusion rates. In most
of its area of distribution, the Assoq Member is overlain
by subaerial lava flows of the upper Rinks Dal Member
(Fig. 131). It is concluded that the Assoq Member generally
correlates with the Rinks Dal Member. On easternmost
central Nuussuaq, however, an outcrop of mudstones
interbedded with invasive lava flows of the younger
Niaqussat Member is also referred to the Assoq Member
(A.K. Pedersen et al. 2002).
Acknowledgements
The work reported on in this publication was carried
out with considerable financial support from the Danish
Energy Research Programme (EFP), the Danish Natural
Science Research Council (SNF), the Bureau of Minerals
and Petroleum, Government of Greenland, the Carlsberg
Foundation and the Arktisk Station, University of Copen -
hagen. Their support is gratefully acknowledged.
The authors are greatly indebted to the three referees:
Dr. T. Christopher R. Pulvertaft, now retired from GEUS,
has taken a keen interest in the manuscript from its early
stages and has encouraged the authors throughout. He
has corrected the English language and has used his great
knowledge of the area to ensure that details in descriptions
and illustrations are correct. Dr. J. Christopher
Harrison of the Geological Survey of Canada and Dr.
Robert Knox of the British Geological Survey have read
the manuscript very carefully and offered a large number
of helpful suggestions for the improvement of text
and figures. With few exceptions, the illustrations have
been prepared by Jette Halskov, GEUS, without whom
the manuscript would not have been completed.
159

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168

Appendix: Place names and localities
The place names and localities mentioned in the text are shown on one or more maps. Figure 2 contains many names and indicates the position
of more detailed maps where the remaining names are shown. Names in italics are names with old spelling. They are located under their
modern spelling or indicated on the historical maps (Figs 3, 4). The old forms of the names are typically mentioned under the heading
‘History’.
Place name
Place name
A
Aaffarsuaq central Nuussuaq Figs 2, 82
Aamaruutissat
(also Skansen) southern Disko Fig. 124
Aasiaat southern Disko Bugt Figs 2, 10
Agatdalen central Nuussuaq Fig. 113
Agatkløft central Nuussuaq Fig. 113
Akuliarusinnguaq (Ak) southern Nuussuaq Fig. 2
Akunneq northern Disko Fig. 124
Alianaatsunnguaq southern Nuussuaq Fig. 2
Alianaitsúnguaq
(now Alianaatsunnguaq) southern Nuussuaq Figs 2, 4
Anariatorfik western Nuussuaq Fig. 65
Angiarsuit northern Nuussuaq Fig. 22
Angiissat
(part of Grønne Ejland) southern Disko Bugt Fig. 2
Angnertuneq
(now Annertuneq)
Annertuneq northern Nuussuaq Fig. 74
Aqajaruata Qaqqaa eastern Disko Fig. 124
Auvfarssuaq
(now Aaffarsuaq)
Assoq southern Disko Figs 2, 124
Asuk northern Disko Fig. 2
Ata (now Ataa) southern Nuussuaq Fig. 4
Atâ (now Ataa)
Ataa southern Nuussuaq Fig. 40
Ataata Kuua southern Nuussuaq Figs 6, 40
Atane (now Ataa) southern Nuussuaq Fig. 3
Atanekerdluk
(now Atanikerluk) southern Nuussuaq Fig. 3
Atanikerdluk
(now Atanikerluk) southern Nuussuaq Fig. 4
Atanikerluk southern Nuussuaq Fig. 40
Atâta kûa
(now Ataata Kuua)
B
Baffin Bay Fig. 1
Blåbærdalen southern Disko Fig. 124
D
Danienrygge (DR) northern Nuussuaq Fig. 74
Daugaard Jensen Dal central Disko Fig. 124
Davis Strait Fig. 1
Disko Figs 2, 10,
124
Disko Bugt Figs 2, 10
Disko Gneiss Ridge
(DGR) western Disko Fig. 10
E
Ekkorfat (now Ikorfat) northern Nuussuaq Fig. 3
Ekorgfat (now Ikorfat) northern Nuussuaq Fig. 4
Eqalulik western Nuussuaq Fig. 65
Eqip Inaarsuata Qaqqaa
(EIQ) eastern Nuussuaq Fig. 2
F
Firefjeld Svartenhuk Halvø Fig. 73
FP93-3-1 northern Disko Fig. 2
FP94-11-02 northern Nuussuaq Fig. 74
FP94-11-04 northern Nuussuaq Fig. 74
FP94-11-05 northern Nuussuaq Fig. 74
FP94-9-01 western Nuussuaq Fig. 65
Frederik Lange Dal eastern Disko Fig. 124
G
GANE#1 western Nuussuaq Fig. 65
GANK#1 western Nuussuaq Fig. 65
GANT#1 northern Nuussuaq Fig. 74
GANW#1 western Nuussuaq Fig. 65
GGU 247701 southern Nuussuaq Fig. 40
GGU 247801 southern Nuussuaq Fig. 40
GGU 247901 southern Nuussuaq Fig. 40
GGU 400701 central Nuussuaq Fig. 113
GGU 400702 central Nuussuaq Fig. 113
GGU 400703 central Nuussuaq Fig. 113
GGU 400704 central Nuussuaq Fig. 113
GGU 400705 northern Nuussuaq Fig. 74
GGU 400706 northern Nuussuaq Fig. 74
GGU 400707 northern Nuussuaq Fig. 74
GGU 400708 Svartenhuk Halvø Fig. 73
GGU 400709 Svartenhuk Halvø Fig. 73
GGU 400710 Svartenhuk Halvø Fig. 73
GGU 400711 Svartenhuk Halvø Fig. 73
GGU 400712 Svartenhuk Halvø Fig. 73
Giesecke Monument southern Nuussuaq Figs 6, 40
169

Place name
Place name
GRO#3 western Nuussuaq Fig. 65
Grønne Ejland southern Disko Bugt Figs 2, 10
Gule Ryg eastern Disko Fig. 124
I
Igdlokungoak
(now Illokunnguaq) northern Disko Fig. 3
Igdlokunguak
(now Illokunnguaq) northern Disko Fig. 4
Igdlunguaq
(now Illunnguaq)
Ikorfat northern Nuussuaq Figs 2, 22
Ikorfat fault zone (Ik) northern Nuussuaq Fig. 10
Illukunnguaq northern Disko Fig. 124
Illunnguaq southern Disko Fig. 124
Ilugissoq central Nuussuaq Fig. 2
Ilulissat eastern Disko Bugt Figs 2, 10
Innanguit southern Disko Fig. 124
Inngigissoq northern Disko Fig. 124
Innaarsuit (also Skansen) southern Disko Fig. 124
Ippigaarsukkløften southern Nuussuaq Fig. 40
Itilli western Nuussuaq Figs 2, 65
Itivnera central Nuussuaq Fig. 82
Itsaku Svartenhuk Halvø Fig. 73
Ivissussat southern Nuussuaq Fig. 40
Ivissussat Qaqqaat southern Nuussuaq Figs 6, 40
Ivisaannguit southern Nuussuaq Figs 6, 40
Ivnanguit (now Innanguit) southern Disko Fig. 4
J.P.J. Ravn Kløft northern Nuussuaq Fig. 22
K
Kaersuarsuk (now Qaarsut)
Kaersut (now Qaarsut) northern Nuussuaq Fig. 4
Kangersooq central Nuussuaq Fig. 82
Kangersôq
(now Kangersooq)
Kangilia northern Nuussuaq Fig. 74
Kardlok
(now Qallunguaq) southern Nuussuaq Fig. 4
Kardlunguaq
(now Qallunguaq)
Karsoq (now Qaarsut)
Killuusat southern Disko Fig. 124
Kingigtok
(now Kingittoq) southern Nuussuaq Fig. 4
Kingigtoq (now Kingittoq)
Kingittoq southern Nuussuaq Fig. 40
Kitdlusat (now Killusat) southern Disko Fig. 4
Kome (now Kuuk) northern Nuussuaq Fig. 3
Kook (now Kuuk) northern Nuussuaq Fig. 4
Kook angnertunek
(now Annertuneq) northern Nuussuaq Fig. 4
Kudliset (now Qullissat) northern Disko Fig. 3
Kûk (now Kuuk) northern Nuussuaq Fig. 21
Kûk quamassoq
(now Kuuk Qaamasoq)
Kussinerujuk northern Disko Fig. 2
Kugannguaq valley northern Disko Fig. 2
Kuugannguaq–Qunnilik Fault
(KQ) western Nuussuaq Fig. 10
Kuuk northern Nuussuaq Fig. 21
Kuuk Qaamasoq southern Disko Fig. 124
Kuussuaq central Nuussuaq Fig. 65
Kvandalen eastern Disko Fig. 124
L
Labrador Sea Fig. 1
Laksedalen eastern Disko Fig. 124
M
Majorallattarfik northern Nuussuaq Fig. 21
Maligaat north-west of Disko Fig. 2
Marraat southern Disko Fig. 124
Marraat-1 western Nuussuaq Fig. 65
Marrait (now Marraat)
Marrak (now Marraat) southern Disko Fig. 4
Melville Bay Fig. 1
N
Naajaat southern Nuussuaq Fig. 40
Naassat central Nuussuaq Fig. 2
Nalluarissat central Nuussuaq Fig. 82
Naujat (now Naajaat) southern Nuussuaq Fig. 4
Naujât (now Naajaat)
Niakornak
(now Niaqornat) northern Nuussuaq Fig. 3
Niakornat
(now Niaqornat) northern Nuussuaq Fig. 4
Niaqornat northern Nuussuaq Fig. 74
Noursoak Halfö
(now Nuussuaq) Fig. 3
Nûgârssuk
(now Nuugaarsuk)
Nûgssuaq
(now Nuussuaq)
Nugsuak
(now Nuussuaq)
Nugsuaks-Halvö
(now Nuussuaq) Fig. 4
Nuugaarsuk northern Disko Fig. 124
Nuuk Killeq southern Nuussuaq Fig. 2
Nuuk Qiterleq southern Nuussuaq Fig. 2
Nuussuaq Figs 2, 10
Nuussuaq Basin Fig. 1
O
Omenak (now Uummannaq) Fig. 3
170

Place name
Place name
P
Paatuut southern Nuussuaq Figs 2, 40
Paatuutkløften southern Nuussuaq Fig. 40
Patoot (now Paatuut) southern Nuussuaq Fig. 4
Pâtût (now Paatuut)
Pautût (now Paatuut)
Peak 1010 m southern Nuussuaq Figs 6, 40
Pingo (now Pingu)
Pingu eastern Disko Figs 2, 124
Pingunnguup Kuua western Nuussuaq Fig. 65
Q
Qaarsut northern Nuussuaq Figs 2, 22
Qaarsutjægerdal central Nuussuaq Fig. 113
Qagdlúnguaq
(now Qallunnguaq)
Qallorsuaq (Keglen) southern Nuussuaq Fig. 40
Qallunnguaq southern Nuussuaq Fig. 40
Qardlok (now Qallunnguaq)
Qeqertarsuaq (island) Figs 2, 10,
73
Qeqertarsuaq (town) southern Disko Figs 2, 10
Qilakitsoq central Nuussuaq Fig. 82
Qorlortorsuaq northern Disko Fig. 2
Quikassaap Kuua southern Nuussuaq Fig. 40
Quikavsaup kûa
(Quikassaap Kuua)
Qutdligssat
(now Qullissat)
Qullissat northern Disko Fig. 2
R
Ritenbenks Kulbrud
(now Qullissat) northern Disko Figs 3, 4
S
Sakkak (now Saqqaq) southern Nuussuaq Fig. 3
Sarkak (now Saqqaq) southern Nuussuaq Fig. 4
Saqqaq southern Nuussuaq Fig. 2
Saqqaqdalen southern Nuussuaq Figs 2, 40
Sarfâgfik northern Nuussuaq Fig. 21
Sarqaq (now Saqqaq)
Scaphitesnæsen central Nuussuaq Fig. 113
Serfat northern Nuussuaq Fig. 74
Sill Sø central Nuussuaq Fig. 113
Sinigfik (now Siniffik) southern Disko Fig. 4
Sinnifik (now Siniffik) southern Disko Fig. 3
Skandsen (now Skansen)
Skansen southern Disko Figs 2, 124
Skarvefjeld southern Disko Fig. 2
Slibestensfjeldet northern Nuussuaq Fig. 22
Sorte Hak central Disko Figs 2, 124
Stordal central Disko Fig. 2
Svartenhuk Halvø Figs 2, 10,
73
T
Talerua northern Nuussuaq Fig. 22
Tartunaq southern Nuussuaq Fig. 40
Teltbæk fault central Nuussuaq Fig. 113
Tuapassuit northern Nuussuaq Fig. 21
Tuapaat southern Disko Fig. 124
Tuapaat Qaqqaat southern Disko Fig. 124
Tunoqqu central Nuussuaq Fig. 82
Tunorqo (now Tunoqqu)
Tunorsuaq northern Nuussuaq Fig. 74
Tupaasat southern Nuussuaq Figs 2, 6
Turritellakløft central Nuussuaq Fig. 113
U
Ujaragsugsuk
(now Ujarassussuk) northern Disko Fig. 4
Ujarattoorsuaq northern Nuussuaq Fig. 22
Ujarasusuk
(now Ujarassussuk) northern Disko Fig. 3
Ujarasussuk northern Disko Fig. 124
Ukalersalik western Nuussuaq Fig. 65
Umanak
(now Uummannaq) Fig. 4
Umiivik-1 Svartenhuk Halvø Fig. 73
Umiiviup Kangerlua Svartenhuk Halvø Fig. 73
Umiussat (now Umiusat)
Umiusat southern Nuussuaq Fig. 40
Upernivik Næs Fig. 33
Upernivik Ø Figs 2, 10
Uppalluk,
Giesecke Monument southern Nuussuaq Figs 6, 40
Uummannaq Figs 2, 10
Uummannaq Fjord Fig. 10
V
Vaigat Figs 2, 10
Vesterfjeld northern Nuussuaq Fig. 22
171